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POTSDAM  SANDSTONE, 

Stand  Rock,  Dalles  of  the  Wisconsin. 


GEOLOGY 


OF 


WISCONSIN. 


SUKYEY  OF  1873-1877, 


VOLUME  II, 

PART  I.  HISTORICAL. 

II.  EASTERN  WISCONSIN. 

III.  CENTRAL  WISCONSIN. 

IV.  LEAD  REGION. 

ACCOMPANIED   BY  AN 

ATLAS  OF  MAPS 


. 

f 

PUBLISHED  UNDER  THE   DIRECTION   OF  THE 

CHIEF   GEOLOGIST, 

BY   THE 

COMMISSIONERS  OF  PUBLIC  PRINTING 

IN  ACCORDANCE  WITH  LEGISLATIVE  ENA'CTMENT. 
1877. 


DAVID  ATWOOD,  MADISON,  SEIFERT,  GUGLER  &  Co.,  MILWAUKEE, 

8TEREOTYPER  AND   PRINTER.  LITHOGRAPHERS. 


A5 

)/.£ 
&A//C 


To  His  Excellency,  the  Hon.  HARBISON  LUDINGTON, 

Governor  of  Wisconsin. 

gIK:  —  It  affords  me  great  pleasure  to  submit  the  following  contri- 
bution toward  the  final  report  of  the  Geological  Survey  of  Wisconsin, 
begun  in  the  year  1873,  and  still  in  progress.  The  manuscript  for 
the  remaining  volumes  is  in  part  prepared,  but  the  completion  of 
certain  portions  is  dependent  upon  field  work  now  being  prosecuted, 
and  must  await  its  conclusion.  An  earnest  effort  will  be  made  to 
complete  the  series  at  as  early  a  date  as  the  proper  execution  of  the 
work  will  permit. 

Most  respectfully,  your  obedient  servant, 

T.  C.  CHAMBEKLIN, 

Chief  Geologist. 
BELOIT,  August  <?, 


PREFACE. 


THE  LAW,  under  whose  authority  the  reports  of  the  Geological  Sur- 
vey are  being  published,  determines  the  character  of  one  volume, 
which,  from  its  nature,  will  most  appropriately  form  the  initial  vol- 
ume of  the  completed  series.  But  as  it  involves  general  conclusions 
that  can  only  be  arrived  at  after  the  completion  of  field  work,  its  ap- 
pearance must  be  delayed  until  that  work  is  accomplished.  It  was 
not  deemed  advisable  on  this  account,  however,  to  defer  the  publica- 
tion of  such  portions  as  could  be  finished,  and  the  present  volume, 
although  nominally  the  second  of  the  series,  appears  first  in  the  order 
of  time. 

Although  its  size  has  been  expanded  beyond  what  was  originally 
intended,  and  a  large  portion  of  its  matter  printed  in  a  smaller  type 
than  is  desirable,  it  has  been  found  impossible  to  include  all  the  ma- 
terial that  has  been  gathered  relating  to  the  regions  reported  upon, 
and  a  considerable  amount  of  manuscript  relating  to  each  of  the  dis- 
tricts has  been  necessarily  omitted,  and  other  portions  condensed  to 
an  undesirable  brevity.  It  is  believed,  however,  that,  notwithstanding 
this,  a  creditable  degree  of  thoroughness  and  fullness  has  been  attained, 
and  that,  by  the  assistance  of  the  ample  maps  and  profiles  that  accom- 
pany the  volume,  an  adequate  knowledge  of  the  structure  of  any 
locality  may  be  obtained. 

The  law  authorizing  the  survey  requires  the  construction  of  a  sin- 
gle map  upon  which  shall  be  represented  all  the  geological  forma- 
tions of  the  state.  A  map  based  upon  a  scale  of  fifteen  miles  to  the 
inch,  is  the  smallest  upon  which  this  can  be  successfully  accomplished, 
and  this  fact  has  determined  the  form  and  dimensions  of  the  accom- 
panying atlas,  whose  sheets  have  the  size  requisite  for  such  a  map. 
A  scale  of  three  miles  to  the  inch  is  the  least  that  is  at  all  adequate 
to  the  proper  representation  of  the  detailed  mapping  of  the  formations, 
and  this  scale  has  been  uniformly  adopted  for  the  more  elaborate  ge- 
ological maps.  It  was  found  that  the  surface  of  the  state,  on  this 
scale,  was  readily  and  economically  divisible  into  rectangles  of  the  size 


vi  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

indicated,  and  these  constitute  the  Area  maps  of  the  atlas.  Seven  of 
these  cover  the  territory  reported  upon  in  this  volume.  At  least  an 
equal  number  will  be  required  for  the  regions  yet  to  be  reported  upon, 
and  these  will  be  numbered  consecutively  with  those  now  published, 
so  that  the  whole  series,  when  complete,  may  form  a  single  portfo- 
lio. The  contour  lines  of  the  topographical  maps  of  the  Lead  region 
required  the  still  larger  scale  of  one  inch  to  the  mile,  and  five  plates 
are  devoted  to  them. 

It  may  be  unnecessary  to  state  that  the  construction  of  an  ordina- 
ry surface  map  is  no  proper  part  of  the  work  of  a  geological  survey, 
and  the  geological  corps  cannot  justly  be  held  responsible  for  errors 
of  a  merely  geographical  nature.  When  it  is  considered  that  the 
original  provisions  of  the  law  required  the  examination  of  more  than 
13,000  square  miles  each  year,  it  will  be  evident  that  no  work  of  that 
kind  was  contemplated.  But  a  correct  geographical  map  is  highly 
important  to  accuracy  in  the  delineation  of  the  formations  sketched 
upon  it,  and  hence  the  corps  have  labored  under  some  annoying  dif- 
ficulties growing  out  of  the  inaccuracies  of  the  original  government  sur- 
veys, and  of  the  maps  in  common  use.  To  overcome  these  difficulties,  so 
far  as  possible,  the  Area  maps  have  been  built  up,  township  by  town- 
ship, from  the  notes  of  the  original  linear  survey  of  the  government, 
and  comparisons  instituted  with  state,  county,  township  and  special 
maps,  and  with  the  observations  of  the  geological  corps.  The  townships 
and  sections  should  be,  setting  aside  the  convergence  of  the  meridi- 
ans and  the  trivial  effects  of  sphericity,  perfect  squares,  and  cover  the 
state  with  a  symmetrical  network  of  lines,  but  it  will  be  observed 
that  there  are  marked  departures  from  this  form  in  some  cases,  due 
to  errors  in  the  linear  surve}7,  and  an  effort  has  been  made,  by  care- 
fully representing  these  on  the  maps,  to  restore  the  natural  features 
to  their  true  form  and  position. 

The  areas  mapped  as  Wet  Lands  are  essentially  those  given  on  the 
government  plats  as  marshes,  but  that  term  is  not  now  properly  ap- 
plicable to  a  considerable  portion  of  the  surfaces  so  designated,  since 
most  of  them  are  so  firm  that  they  may  be  readily  traversed  by  teams, 
and  some  are  even  cultivated  with  success  in  all  except  very  wet  sea- 
sons, and  are,  indeed,  among  the  most  valuable  lands  of  the  state.  In 
the  great  majority  of  cases,  except  where  they  are  flu  viatile  meadows, 
they  represent  extinct  lakes,  and  hence  their  historical  and  geologi- 
cal significance  is  important. 

The  survey  has  been  put  under  great  obligations  by  the  kindness 
of  citizens  and  corporations  in  rendering  valuable  aid  in  various  ways 
in  the  prosecution  of  the  work.  In  addition  to  the  more  specific  ac- 


PREFACE.  vii 

knowledgments  that  have  been  made  in  connection  with  the  annual 
reports  and  in  other  appropriate  ways,  the  corps  desire  to  tender  this 
general  expression  of  their  appreciation  of  the  numerous  courtesies 
of  which  they  have  been  the  recipients. 

It  is  due  also  to  those  whose  results  do  not  appear  in  an  individual- 
ized form,  to  call  attention  to  the  analytical  work  of  Prof.  "W.  W. 
Daniells,  of  the  State  University;  of  Mr.  Gustavus  Bode,  of  Milwau- 
kee; and  of  Mr.  E.  T.  Sweet,  recently  of  Madison;  to  the  paleonto- 
logical  identifications  of  Prof.  R.  P.  Whitfield,  of  New  York,  and  to 
the  drafting  of  Prof.  W.  J.  L.  Nicodemus  and  Mr.  A.  D.  Coriover,  of 
the  State  University. 

An  expression  of  indebtedness  is  also  due  Prof.  R.  P.  Whitfield, 
lion.  Geo.  H.  Paul,  Prof.  A.  Salisbury,  G.  D.  Swezey,  J.  H.  Cham- 
berlin  and  0.  S.  Bacon,  for  reading  portions  of  the  proof  on  subjects 
with  which  they  are  especially  familiar. 

The  provision  which  has  been  made  by  the  commissioners  of  pub- 
lic printing  for  the  publication  of  the  work  has  proved  wise  and 
judicious,  as  well  as  highly  economical. 

The  mechanical  execution  of  the  work  is  the  best  witness  that  can 
be  offered  as  to  the  skill  and  faithfulness  with  which  the  printers  and 
lithographers  have  performed  their  respective  tasks.  The  execution 
of  large. geological  maps  is  confessedly  a  work  of  much  difficulty,  and 
great  credit  is  due  the  lithographers  for  the  obliging  and  liberal  man- 
ner in  which  they  have  performed  their  work.  In  several  instances 
they  have  exceeded  the  requirements  of  their  contract. 


TABLE  OF  CONTENTS. 


LETTER  OF  TRANSMITTAL, ....-in 

PREFACE, _-------     v 

PAET  I. 

HISTORICAL. 
PREFATORY  NOTE, 3 


ANNUAL  REPORT  FOR  1873. 

BY  I.  A.  LAPHAM. 

Law  of  the  Survey  —  Organization  of  the  Corps  —  Prof.  Irvrng's  Party  —  Prof.  Cham- 
berlin's  Party  —  Mr.  Strong's  Party  —  Mr.  Wilson's  Map  —  Practical  Importance 
of  Geological  Knowledge  —  Mr.  Edgerton's  Survey  —  Topographical  Survey  — 
Railroad  Elevations  —  Elevation  of  Lakes  —  Elevation  of  Summits  —  Government 
Surveys  —  Catalogue  of  Minerals  —  Mineral  Waters  —  Rain  Fall —  Relation  of  the 
Geological  Survey  to  Agriculture —  List  of  Maps  Accompanying  the  Report,  5-44 

ANNUAL  REPORT  FOR  1874. 

BY  I.  A.  LAPHAJI. 

Details  of  Progress  —  Prof.  Irving's  Party  —  Prof.  Chamberlin's  Party — Mr.  Strong's 
Party  —  Surveys  in  Oconto  County  by  Maj.  Brooks  —  Determinations  of  Latitude 
and  Longitude  by  the  U.  S.  Engineer  Department  —  Geodetic  Survey  under  Dr. 
Davies  —  Mr.  Ives'  Survey  —  Chemical  Work  —  List  of  Maps  and  Sections  Accom- 
panying the  Report  —  List  of  Papers  Accompanying  the  Report,  -  -  45-66 

ANNUAL  REPORT  FOR  1875. 

BY  O.  W.  WIGHT. 

Brief  History  of  Previous  Geological  Surveys  in  Wisconsin  —  Reconnoissance  made  in 
the  Northern  Part  of  the  State  under  the  Personal  Direction  of  the  Chief  Geologist, 
During  the  Latter  Portion  of  the  Season  of  1875  —  Hamilton,  or  Lower  Helder- 
burg  —  Artesian  Wells  —  Mineral  Springs  —  Acknowledgements,  -  -  67-89 


X  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

PAKT  II. 
GEOLOGY  OF  EASTERN  WISCONSIN. 

BY  T.  C.  CHAMBEKLIN. 

ACKNOWLEDGEMENTS,       -  -       93 

EXTENT  OF  DISTRICT,  94 

PREVIOUS  PUBLICATIONS  RELATING  TO  THE  REGION,    -  -       95 

CHAPTER  L  — TOPOGRAPHY. 

Preglacial  Features  —  Glacial  Features  —  Postglacial  Features  —  General  Slopes  —  Pe- 
culiar Diagonal  Valley  —  The  Fox  River — Its  Commercial  Importance  —  Origin  — 
Rock  River  Valley  —  Peculiarities  of  its  Course  —  Commercial  Importance  —  Valley 
of  Lake  Michigan  —  Slopes  and  Dividing  Ridges  —  Kettle  Range  —  Elevations, 

95-127 

CHAPTER  II.  — HYDROLOGY. 

DRAINAGE — The  Watershed  —  The  Mississippi  and  St.  Lawrence  Basins  —  Peculiar- 
ities of  Streams  of  Walworth  and  Adjacent  Counties  —  Of  the  Pike  River  —  Of  the 
Milwaukee  River  —  Of  the  East  Twin  River  —  Of  the  Wolf,  Oconto,  Peshtigo  and 
Menomonee  Rivers  —  Of  the  East  Branch  of  the  Rock  River  —  Relationship  of  some 
of  the  Streams  on  Opposite  Sides  of  the  Kettle  Range  —  Geneva  Lake  and  Big  Foot 
Prairie  —  Delavan  Lake  and  White  River — Turtle  Creek  and  Sugar  Creek  —  Bark 
and  Oconomowoc  Rivers  and  the  Branches  of  Cedar  Creek  —  Rubicon  River  and 
Cedar  Creek  —  Origin  and  Geological  Relations  of  the  Lakes  of  Eastern  Wiscon- 
sin —  Lake  Michigan  —  Green  Bay,  Lake  Winnebago  and  the  Former  Lake  Hori- 
con  —  Lake  Poygan  —  Lake  Puckawa  —  Green  Lake  —  Rush  Lake  —  Lake  Sha- 
wano  —  Lake  Koshkonong  —  Glacial  Lakes  —  Moraine  Lakes  —  Minor  Lakes  — 
Their  Beauty  and  Value  —  Geneva,  Oconomowoc,  Green,  Elkhart,  Rock,  Brown, 
Clear  and  Delavan  Lakes  —  Water  Supply  —  Springs  —  Two  General  Systems  — 
The  Several  Geological  Horizons  — Analyses  —  Source  of  Mineral  Substances —  Medi- 
cinal Character — Sulphur  Springs — Chalybeate  Springs — Travertine  Springs — Trout 
Springs — Artesian  Wells  —  Classified  According  to  Source  of  Flow  —  Fountains  at 
Fond  du  Lac  —  At  Taycheedah  —  In  Byron  —  In  Oakfield  —  At  Oshkosh  —  In  Cal- 
umet—  In  Rushford,  Aurora  and  Poysippi — At  Watertown  —  At  Pahnyra  —  At 
Whitewater  —  At  Manitowoc  —  At  Western  Union  Junction  — At  Racine  —  At  Mil- 
waukee —  At  Sheboygan  —  At  Janesville  —  Possibilities  of  Obtaining  Fountains  at 
Other  Points  —  The  Three  Districts  —  Elevations  of  Junction  of  St.  Peters  Sand- 
stone and  Trenton  Limestone  —  Water  Power  —  Of  Rock  River  —  Of  the  Fox 
River — Of  the  Wolf,  Oconto,  Peshtigo  and  Menomonee  Rivers  —  Of  Milwaukee, 
Sheboygan  and  Manitowoc  Rivers  —  Changes  in  Drainage,  -  -  128-175 

CHAPTER  III.  — NATIVE  VEGETATION. 

Agricultural  Indications  —  Natural  Grouping  of  Plants  —  Upland  Vegetation,  Prairie 
Group  —  Oak  Group — Oak  and  Maple  Group  —  Maple  Group  —  Maple  and  Beach 
Group  —  Hardwood  and  Conifer  Group  —  Pine  Group  —  Limestone  Ledge  Group — 
Comprehensive  Group  —  Marsh  Vegetation  —  Grass  and  Sedge  Group  —  Heath 
Group  —  Tamarac  Group —  Arbor  Vitas  Group —  Spruce  Group  —  Black  Ash  Group — 
Yellow  Birch  Group — Distribution — Cranberries  —  Native  Occurrence  —  Condi-/ 
tions  of  Success  in  Culture,  -  -  -  -  -  -  -  -  176-1 7$ 


TABLE  OF  CONTEXTS.  xi 

CHAPTER  IV.— SOILS. 

Origin  — Classes  of  Soils  — Prairie  Loam  —  Lighter  Marly  Clay  Soils  —  Heavier  Marly 
Clay  Soils  —  Red  Marly  Clay  Soils  —  Limestone  Loam  —  Silicious  Sandy  Soils  — 
Calcareous  Sandy  Soils  — Humus  Soils  —  Alluvial  Soils  —  Analyses  of  Soils  —  Mag- 
nesian  Character  —  Comparison  of  Soils  and  Vegetation,  -  188-198 

CHAPTER  V.  — QUATERNARY  FORMATIONS— THE  DRIFT. 

Definition  —  Glacial  Movements — Direction  of  Glacial  Grooves  —  Trains  of  Bowlders 
from  Archsean  Outcrops  —  Surface  Configuration  —  Peculiar  Phenomena  at  Burling- 
ton and  East  Troy  —  Fiords  —  Glacial  Drift,  Moraines,  Kettle  Range  —  ' '  Kettles  ' ' 

—  Character  of  Range  — Width  —  Material  —  Structure  —  Comparative  Abruptness 
of  Opposite  Slopes  —  General  Relationship  —  Summit  Altitudes  —  Kettle  Range,  a 
Gigantic  Moraine  — Minor  Moraines — Bowlder  Clay  or  Till  —  Origin  — Composition 

—  Gravel  Bowlders  —  Modified  Drift,   Champlain,   Beach  Formation  A.  —  The 
Lower  Red  Clay  —  Character — Thickness  —  Elevations  it  Attains,  and  their  Sig- 
nificance —  Depression  indicated  —  Beach  Formation  B.  —  Character  —  Thickness 

—  Upper  Red  Clay  —  Character — Thickness  —  Beach  Formations  C.  and  D.,  and 
the  Modified  Red  Clay  —  Description  —  Relations  —  Origin  —  Altitudes  of  the  Beach 
Ridge — Terraces  —  Beach  Ridge  of  Sand — Beach  Ridge  of  Rock- Fragments  — 
Terraces  of   Rock — The   Three   Forms  United  —  Secondary  Beach  Lanes  —  Gen- 
eral Movements — Encroachments  of  Lake  Michigan  —  Dunes — Erosion  and  Deposit 

—  Industrial  Nature  of  the  Drift  Formations  —  Brick  —  Chemical  Nature  of  the 
White  Brick  —  Manufacture  at  Milwaukee,  Racine,  Ozaukee,  Sheboygan  Falls, 
Manitowoc,  Kewaunee,  Appleton,  Neenah,  Menasha,  Clifton,  Watertown,  Water- 
loo, Jefferson,  Ft.  Atkinson,  Edgerton,  Whitewater,  and  elsewhere  —  Tiles  —  Pot- 
tery—  Magnetic  Iron  Sands  —  Shell  Marl — Peat  —  Origin  —  Details  of  Borings  — 
Utilization,  -      199-246 

FORMATIONS  OP  EASTERN  WISCONSIN,         -  -  '        247 

CHAPTER  VI.  — ARCHAEAN  FORMATIONS. 

The  Mukwa    Granite  —  The  Berlin  Porphyry  —  The  Quartz-Porphyry  of  Pine  Bluffh 

—  The  Quartz-Porphyry  of  Marquette  —  The  Quartzites  of  Portland  and  Water- 
loo, -      248-256 

CHAPTER  VII.— LOWER  SILURIAN. 

POTSDAM  SANDSTONE  —  General  Character — Madison  Sandstone  —  Mendota  Limestone 

—  Organic  Remains  —  Method  of  Deposit  —  Extent  —  Sections  and  Local  Descrip- 
tions—  Lower  Maanesian  Limestone  —  General  Character  —  Organic  Remains  — 

.  Area  —  Thickness  —  Local  Descriptions  —  Economic  Considerations  —  St.  Peters 
Sandstone  —  Thickness  —  Structure  —  Transition  Beds  —  Organic  Remains  —  Meth- 
od of  Formation  —  Extent  and  Local  Descriptions  —  Economic  Considerations  — 
Trenton  Group  —  Trenton  Limestone  —  Subdivisions — Lower  Buff  Beds  —  Lower 
Blue  Beds  —  Upper  Buff  Beds  —  Upper  Blue  Beds  —  Local  Descriptions  —  Indus- 
trial Considerations  —  Galena  Limestone  —  General  Characteristics  —  ( )rganic  Con- 
tents —  Thickness  —  Industrial  Value  —  Distribution  and  Local  Details  —  Recapitu- 
lation— The  Cincinnati  Shales  and  Limestones  —  General  Character  —  Thickness 

—  Life  —  Industrial  Value  —  Distribution  and  Local  Details  —  Table  of  Fossils  of 
the  Trenton  Period,  .......      257-326 


xii  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

CHAPTER  VIII  — UPPER  SILURIAN. 

CLINTON  IRON  ORE  DEPOSIT  —  Age  and  Stratigraphical  Relations  —  Formation  at 
Iron  Ridge  —  Analyses  —  Product  —  Furnaces  —  Formation  at  Hartford  —  In  Stock- 
bridge —  Near  De  Pere  —  General  Conclusions  —  Niagara  Limestone  —  Subdivis- 
ions—  Mayville  Beds  —  Character  —  Analyses  —  Life  —  Table  of  Fossils  —  Econ- 
omic Value  —  Distribution  and  Local  Descriptions  —  Byron  Beds  —  Character  — 
Analyses  —  Fossils  —  Thickness  —  Distribution  —  Economic  Considerations  —  Trans- 
ition Beds  —  Lower  Coral  Beds  —  Nature  —  Organic  Remains  —  Table  of  Fossils  — 
Upper  Coral  Beds  —  Nature  —  Organic  Remains  —  Table  of  Fossils  —  Distribu- 
tion —  Local  Details  — Waukesha  Beds  —  Character  —  Development  at  Waukosha, 
at  Pewaukee,  in  Genesee,  elsewhere  —  Racine  Beds  —  Extent  and  Relations  — 
Local  Details  —  Summation  —  Conclusions  —  Coral  Reefs  —  Organic  Remains  — 
Table  of  Fossils  —  Guelph  Beds  —  Nature  —  Local  Details  —  Table  of  Fossils  —  In- 
dustrial Value  of  tfie  Waukesha,  Racine,  and  Guelph  Beds  —  Lime  —  Analyses  — 
Building  Stone  —  Flux — Table  of  Fossils  of  the  Niagara  Group  —  Lower  HeJder- 
berg  Limestone  —  Character — Analyses  —  Extent  —  Fossils  —  Formation  in  Fre- 
donia  —  Fossils  —  Analyses  —  Conclusions  —  Economic  Considerations,  -  327-39-i 

CHAPTER  IX  — DEVONIAN. 

HAMILTON  CEMENT  ROCK  —  Nature  —  Composition  —  Analyses  —  Organic  Remains  — 
Description  of  New  Species  of  Fish  —  Age  of  Formation  —  Local  Descriptions  — 
Economic  Considerations  —  Investigations  on  the  Hydraulic  Properties  of  the  For- 
mation, -. 395-405 

PART  III. 
GEOLOGY  OF  CENTRAL  WISCONSIN. 

BY  ROLAND  D.  IRVING. 

INTRODUCTION  —  Extent  of  District  —  Previous  Investigations  —  Arrangement  of  Re- 
port—  Acknowledgments 408-412 

CHAPTER  I.  — SURFACE  FEATURES  OF  CENTRAL  WISCONSIN. 

RIVER  SYSTEMS  AND  GENERAL  SURFACE  SLOPES  —  The  Wisconsin  River  —  Table  of 
Altitudes  of  Water  Surface  of  Wisconsin  River  —  The  Black  River — The  Rock 
River  —  The  Fox  River  —  Fall  of  Fox  River.  —  Surface  Reliefs  —  Watersheds  — 
Baraboo  Bluffs  —  Isolated  Peaks  and  Ridges  — Altitudes,  Madison  to  Elroy  —  Elroy 
to  Merrillon  —  Waterloo  to  Madison  —  Edgerton  to  Black  Earth  —  Camp  Douglas 
to  Randolph  —  Tomah  to  Wausau  —  Amlierst  to  Merrillon  —  Portage  to  Stevens 
Point —  Stevens  Point  to  North  Line  of  Township  29  —  BAROMETRICAL  ALTITUDES 

—  Relations  of  the  Topography  to  the  Geology  of  the  region —  Vegetation  and  Soils 

—  Praines  —  Marshes  and  Timber  Land  —  Topographical  Subdivisions  —  Resume. 
Region   of  Crystalline  Rocks  —  Central  Sandstone  Region  —  Limestone  District, 

413-456 

CHAPTER  II.— GENERAL  GEOLOGICAL  STRUCTURE  OF  CENTRAL 

WISCONSIN. 

Laurention  System  —  Huronian  System  —  Silurian  Formations  —  Glacial  Drift  —  Table 
of  Formations 457-460 


TABLE  OF  CONTEXTS.  xiii 

CHAPTER  III.— THE  ARCH.EAN  ROCKS. 

The  Main.  Arch-jean  Area  —  Considered  in  General  —  Line  of  Junction  with  Potsdam  — 
Unconf 01  inability — Topographical  Features  of  the  Crystalline  Rock  District  — 
Kind  of  Rocks  —  Bedding  —  Intrusive  Granite  —  Weathering  —  Strike  —  Laur- 
entian  —  Huronian  —  Economic  Importance  —  Local  Details  —  In  Upper  Wisconsin 
Valley  —  In  Yellow  River  Valley — In  Black  River  Valley  —  Isolated  Archtean 
Areas  —  In  General  —  Table  of  Isolated  Archffian  Outcrops  —  Special  Descriptions 

—  The    Baraboo    Quartzite    Ranges  —  The    Marcellon    Quartz-Porphyry  —  The 
Observatory    Hill    Quartz-Porphyry  —  The    Moundville    Quartz-Porphyry — The 
Seneca    Quartz-Porphyry  —  The  Marquette  and  Berlin  Quartz- Porphyries  —  Com- 
parison of  the  Rocks  of  the  Several  Porphyry  Areas  —  The  Montello  Granite  — 
The  Marion  Granite  Areas  —  Conclusions  —  The  Necedah  Quartzite      -        461-524 

CHAPTER  IV  — THE  LOWER  SILURIAN  ROCKS  CONSIDERED  IN  GENERAL. 

POTSDAM  SANDSTONE  SERIES  —  Mendota  Limestone  —  Madison  Sandstone  —  Two 
Names  —  Former  Investigation  —  Surface  Distribution  —  Boundary  Between  Pots- 
dam and  Archaean  Areas  —  Between  Potsdam  and  Lower  Magnesian  Areas  —  To- 
pographical Characters — Lithological  Characters  and  Stratigraphical  Arrangement 

—  Sections  —  Analysis  of  Greensand  —  Discussion  of  Anomalous  Relations  of  Cer- 
tain Portions  of  the  Formation  —  Beds  of  Passage  —  Madison  and  Mendota  Beds  — 
Analyses  —  Fossils  —  Economic  Contents — The  Lower  Magnesian    Limestone  — 
Name  —  Surface  Extent  —  Topographical  Characters  —  Lithological  Characters  — 
Stratigraphical  Arrangement  —  Sections  —  Irregular    Upper    Surface  —  Fossils  — 
Economic  Contents  —  The  Upper  or  St.  Peters  Sandstone  —  Name  —  Distribution 

—  Topographical  Features  —  Lithological  Characters  — Thickness  —  Economic  Con- 
tents —  The  Trenton  Limestone  — Relations  —  Surface  Distribution  —  Topograph- 
ical Characters  —  Lithological  Characters  —  Buff  Limestone  —  Blue  Limestone  — 
Fossils  —  Economic  Contents  —  Building  Stone  —  Flux  —  Galena  Limestone  —  Lo- 
cal Details  —  Portage,  Wood,  Clark  and  Jackson  counties — Juneau  and  Adams 
counties  —  Marquette  and  Waushara  counties,  and  Green  Lake  county  north  of  the 
Fox  river — Sauk  and  Columbia  counties  —  Dane  county.  -     525-607 

CHAPTER  V  — THE  QUATERNARY  DEPOSITS. 

THE  GLACIAL  DRIFT  —  The  Driftless  region  —Outline  of  the  Driftless  Region  — Topo- 
graphy of  the  Driftless  Area  —  Its  Altitude  —  Surface  Features  of  the  Drift- 
beaxing  Regions  —  Linear  Topography— Roches  Moutonees  —  Drift  Hills  and 
Ridges  —  Kettle  Range  —  Materials  of  the  Drift  —  Bowlders  —  Gravel  —  Sand  — 
Clay  —  Arrangement  of  the  Drift  Materials  —  Amount  —  Directions  of  the  Glacial 
movement  —  Table — Origin  and  Directions  of  Travel  of  Erratics  and  Pebbles  —  Or- 
igin of  Sand  and  Clay  of  Drift  —  Economic  Contents  of  Drift  —  Conclusions,  609-636 

APPENDIX  — MICROSCOPIC  LITHOLOGY. 

BY   CHAS.    E.    WRIGHT. 

Silicious  Hornblende  Schist  —  Granite  —  Argillo-chloritic  Schist — Hornblende  Rock  — 
Syenite  —  Silicious  Chloritic  Schist  —  Chloritic  Hornblende  Rock  —  Syenitic  Granite 

—  Silicious  Hornblende  Schist — Chloro-silicious  Schist,        ...        637-039 


xiv  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

PART  IV. 
GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

BY  MOSES  STRONG. 

CHAPTER  I.  — INTRODUCTORY  AND  HISTORICAL. 

Territory  Examined  in  1873  — Plan  of  Operations— Territory  Examined  in  1874—  Pre- 
vious Publications  and  Surveys  —  Survey  of  G.  W.  Featherstonhaugh,  1834-35  — 
Surveys  of  Dr.  D.  D.  Owen  in  1839  and  in  1847-8  — Report  of  E.  Daniels,  1854— 
Survey  of  Prof.  J.  G.  Percival,  1854  to  1856  — Report  of  E.  Daniels,  1858  — Report 
of  Profs.  Hall  and  Whitney,  1862  — Report  of  Rev.  J.  Murrish,  1872  —  Topograph- 
ical and  Geological  Maps  and  Sections  —  Barometrical  Observations  —  Information 
Derived  from  them  —  Elevations  of  Towns  and  other  Localities  —  Acknowledg- 
ments,    645-651 

CHAPTER  II.— TOPOGRAPHY  AND  SURFACE  GEOLOGY. 
GENERAL  FEATURES  OF  THE  COUNTRY — Drainage — Situation  of  the  Dividing  Ridges  or 
Water-sheds — Streams — Theory  of  the  Formation  of  the  Streams  of  the  Lead  Region 

—  Process  of  Erosion  —  Formation  of  the  Wisconsin  River  and  its  Tributaries  —  Re- 
•    suits  of  the  Denudation  —  Diminution  of  Water  in  the  Lead  Region  —  Sinking  of 

Streams  in  Grant  County  —  Causes  of  the  Decrease  of  Water  —  Springs  and  Wells 

—  Springs  of  the  West  Blue  Mound  —  Inorganic  Salts  Contained  in  the  Water  — 
Analysis  —  Prairie  and  Forest  —  Mounds  —  Sinks  —  Soil  and  Subsoil  —  Absence  of 
Drift  —  Distribution  of  the  Surface  Soil  and  Rock  —  Peat  —  Brick  Clay  —  Drift  — 
Gravel  Beds—  Drift  Clay  —  Erratic  Bowlders  of  Sandstone,         -        -        652-667 

CHAPTER  III.— GEOLOGICAL  FORMATIONS. 

Potsdam  Sandstone — Geographical  Boundaries  — Lithological  Characteristics  —  Section 
at  Lone  Rock  —  Coloring  Matter  in  the  Potsdam  —  Hydraulic  Shales  —  Localities  of 
Fossils  —  Lower  Magnesian  Limestone  —  Geographical  Boundaries  —  Lithological 
Characteristics  —  Varying  Thickness — Localities  of  Fossils  —  St.  Peters  Sandstone  — 
Geographical  Boundaries  —  Lithological  Characteristics  —  Terraces — Knobs — Ripple 
Marks  —  Varying  Thickness  —  Upheavals  —  Concretions  —  Induration  on  Exposure 

—  Quarries  —  Trenton  Limestone  —  Geographical  Boundaries  —  Lithological  Char- 
acteristics —  Carbonaceous  Shale  —  Analyses  —  Section  —  Disappearance  of  the  Blue 
Limestone  —  Ores  —  Minerals  —  Organic  Remains  — Galena  Limestone  —  Geograph- 
ical Boundaries  and  Area  —  Lithological  Characteristics  —  Flint — Building  ~S tone — • 
Paleontology  —  Cincinnati  Group — Geographical  Boundaries  and  Area  —  Litholog- 
ical Characteristics  —  Section  —  Localities  of  Fossils,        ...  668-688 

CHAPTER  IV.— THE  LEAD  REGION. 

Boundaries  and  Area  —  Explanation  of  Mining  Terms  —  Mineralogy  —  Paragenesis  of 
Minerals  —  Pseudomorphs  —  Present  Condition  of  the  Mines  —  Section  of  the  Min- 
ing Openings  —  Beetown  District  —  Potosi  District  —  Fairplay  District — Hazel 
Green  District  —  Buncome  Diggings  —  New  Diggings  District  —  Shullsburg  Dis- 
trict —  Benton  District  —  Platteville  District  —  Whig  Diggings  —  Big  Patch  Dig- 
gings— Mifflin  District  —  Centerville  District  —  Blue  River  Paint  Works  —  Highland 
District  —  Linden  District —  Dodgeville  District  —  Porter's  Grove  Digging?  —  Van 
Meter's  Survey  —  Mineral  Point  District  —  Diamond  Grove  Diggings  —  Calamine 
District — Wiota  District — Monroe  District — Occurrence  of  Copper  in  the  Lead 
Region  —  Statistics  of  Zinc  Ore  —  Statistics  of  the  Production  of  Lead  Ore  in  the 
Several  Districts  for  each  year  since  1861 ;  and  the  Smelting  Facilities  —  Concluding 
Remarks, 689-752 


TABLE  OF  CONTENTS.  xv 

ATLAS   PLATES 

ACCOMPANYING  THIS  VOLUME. 

NOTE.  —  As  maps  will  accompany  the  other  volumes  of  this  report,  it  has  been  thought  best  to  arrange 
and  number  the  whole  series  as  one  set,  for  convenience  of  reference  and  binding,  and  hence  the  accom- 
panying atlas  begins  with  Plate  III. 

PLATE. 

III.  Map  of  Soils  and  of  Vegetation  of  Eastern  Wisconsin. 

IV.  Map  of  Topography  and  of  the  Quaternary  Formations  of  Eastern  Wisconsin. 
V.  Map  of  Geology  and  Topography  of  the  Lead  Region. 

VI.  Map  of  Geology  and  Topography  of  the  Lead  Region. 

VII.  Map  of  Geology  and  Topography  of  the  Lead  Region. 

VIII.  Map  of  Geology  and  Topography  of  the  Lead  Region. 
IX.  Map  of  Geology  and  Topography  of  the  Lead  Region. 

X.  Area  A.  —  Geological  map  of  Kenosha,  Racine,  Milwaukee,  Waukesha,  Wai- 
worth,  Jefferson,  and  parts  of  Rock,  Dodge,  Washington  and  Ozaukee  counties. 
XI.  Area  B.  —  Geological  map  of  Fond  du  Lac,  Sheboygan,  Manitowoc,  Calumet, 
Winnebago,  and  parts  of  Dodge,  Washington,  Ozaukee,  Kewaunee,  Brown, 
Outagamie  and  Waupaca  counties. 

XII.  Area  C.  —  Geological  map  of  portions  of  Brown,  Door,  Kewaune*,  Outagamio, 
Shawano  and  Oconto  counties. 

XIII.  Area  D.  —  Geological  map  of  Green,  and  parts  of  Iowa,  La  Fayette,  Dane,  Sauk 

and  Rock  counties. 

XIV.  Area  E.  —  Geological  map  of  Juneau,  Adams,  Waushara,  Marquette,  Sauk,  Col- 

umbia, Green  Lake  and  part  of  Dodge  counties. 
XV.  Area  F.  —  Geological  map  of  Wood,  and  parts  of  Clark,  Jackson,  Marathon  and 

Portage  counties. 

XVI.  Area  G.  — Geological  map  of  Grant,  and  parts  of  La  Fayette,  Iowa,  Richland  and 
Crawford  counties. 


LIST  OF  ILLUSTRATIONS. 

LITHOGRAPHIC  PLATES. 

NOTE.  — The  chromo-lithographs  were  carefully  reproduced  from  photographs. 

PLATE  I.    View  of  Stand  Rock,  Dalles  of  the  Wisconsin  —  Potsdam  Sand- 
stone,     .--_.       Frontispiece. 

Page. 

I  A.    False  Bedding  —  Potsdam  Sandstone  —  Dalles  of  the  Wisconsin,  Opp.    45 
II.    Map  showing  the  Areas  examined  by  the  Several  Parties,  1873- 

1876,                                                                                         -  Opp.    94 
II  A.    Lucas  Point,  Green  Lake,  showing  Junction  of  Potsdam  sandstone 

and  Lower  Magnesian  limestone,       -----  Qpp.    91 

III.  Iron  Ridge  Mine, Opp.  327 

IV.  Topographical  Map  of  Eastern  Wisconsin,    -        ...  Opp.    97 
V.    Profiles  elucidating  Artesian  Fountains  in  Eastern  Wisconsin,  Opp.  151 

VI.    Profiles  elucidating  Artesian  Fountains  in  Eastern  Wisconsin,        Opp.  160 


XVI 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


PLATE.  Page. 

VI  A.    Topographical  Map  of  Milwaukee  County,         .-.._•.•-  Opp.  127 
VII.    Diagram  showing  Glacial  Movements  in  Eastern  Wisconsin,      -  Opp.  204 
VIII.     Profile  Section  of  Quaternary  Formations  along  Lake  Michigan,  Opp.  219 
IX.    Map  showing  Outline  of  Eastern  Wisconsin  during  the  Cham- 
plain  period,          ---------  Opp.  223 

XL    Topographical  map  of  Iron  Eidge  Mining  Property,  Opp.  328 

XII.    Profile  Sections  showing  the  Subdivisions  of  the  Niagara  Group, .  Opp.  336 

XIII.  Profile  Section  through  Artesian  Wells  at  Western  Union  Junc- 

tion, Milwaukee  and  Sheboygan, Opp.  335 

XIII  A.    View  of  Milwaukee  cement  quarry, Opp.  395 

XIV.  View  of  Roche  a  Cris  Bluff,  Potsdam  sandstone,  Opp.  525 
XV.    Archaean.    View  of  Devil's  Lake  and  Kirk's  Bluff,    -        -        -  Opp.  407 

XVI.    Map  of  Centra]  Wisconsin,  showing  the  Hydrographic  Basins  and 

principal  Topographical  Subdivisions, Opp.  453 

XVII.    Map  showing  the  formations  along  Black  river,  Jackson  county,  Opp.  493 

XVIII.    Map  of  Isolated  Archaean  Areas, Opp.  501 

XIX.    Maps  and  Cross  Sections  illustrating  the  Structure  of  the  Devil's 

Lake  Gorge,          -  Opp.  507 

XX.     Cross  Sections  in  Sauk  county, Opp.  590 

XXII.     East  and  West  Sections  in  Columbia  county,      -        ...  Opp.  579 

XXIII.  North  and  South  Sections  in  Columbia  county,        ,        -        -  Opp.  581 

XXIV.  North  and  South  Sections  in  Dane  county,          ....  Qpp.  597 
XXV.    East  and  West  Sections  in  Dane  county,        -  Opp.  600 

XXV  A.    Map  of  part  of  Wisconsin,  showing  glacial  Drift  and  other  Quat- 
ernary formations,          - Opp.  608 

XXVI  A.    Geological  map  of  the  Four  Lake  Country  of  Dane  county,  show- 
ing the  Directions  and  Effects  of  the  Glacial  Movements,      -  Opp.  613 
XXVI.    View  of  bluff  of  Galena  limestone  near  Cassville,  on  the  Missis- 
sippi, Opp.  643 
XXVII.     Outline  map  of  the  Lead  region,  exhibiting  the  Drainage  and  the 

Distribution  of  Prairie  and  Forest Opp.  652 

XXII.    Map  of  Hendy,  Davey,  Sobey  &  Co.'s  mine, ,  Opp.  731 
XXIX.     Section  through  the  Mining  Districts  of  Beetown,  Potosi  and  Fair- 
play,  from  the  mouth  of  the  Mississippi  to  the  State  Line,  show- 
ing the  Denudation,  Opp.  667 

XXX.    Map  of  Linden  mine, *        -  Opp.  726 

XXX  A.    View  of  Bluffs  on  the  Mississippi,  Opp,  689 
XXXI.    Section  through  the  Mining  Districts  of  Hazel  Green,  Benton  and 
Mineral  Point,  from  the  State  Line  to  the  Wisconsin  river, 
showing  Denudation,  Opp.  668 
XXXII.    Outline  map  of  the  Lead  region,  showing  the  several  Mining  Dis- 
tricts and  the  Furnaces,        -        -        -        -        -        -        -  Opp.  742 


FIGURES. 

REPORT  ON  EASTERN  WISCONSIN. 

1.  Geological  Relations  of  Green  Bay  Valley, 

2.  Striated  Cone  of  Limestone,  Pewaukee, 

3.  Trains  of  Bowlders  from  Portland  and  Waterloo  Quartzite  Outliers, 

4.  Peculiar  Glacial  Phenomena  at  Burlington,         .... 


Page. 
101 
200 
202 
203 


TABLE  OF  CONTENTS.  xvii 

Faije, 

5.  Section  of  Kettle  Range  near  Whitewater, 209 

6.  Profile  Across  Kettle  Range,  from  Eagle  Westward, 

7.  Profile  Across  Kettle  Range  near  Whitewater,  Showing  Position  of  Kettles,  211 

8.  Map  of  Moraine  in  Towns  of  Herman  and  Theresa,     -----  215 

9.  Section  of  Moraine  in  Town  of  Herman, 216 

10.  Map  of  Moraine  in  Beloit, 217 

11.  Section  of  Drift  Showing  Gravel  Bowlders,          -        -        -        ..        -        -  219 

12.  Sections  of  Drift  near  Milwaukee, 220 

13.  Section  of  Drift  near  Manitowoc,        ------- 

14.  Section  of  Drift  near  Racine,      -        -        -        -      ^ 227 

15.  Section  Illustrating  Drift  Formation  near  Racine, 227 

16.  Diagram  Illustrating  Movements  of  Drift-Depositing  Agencies,           -        -  230 

17.  Profile  Section  Showing  the  Relations  of  the  Mukwa  Granite,      -        -        -  249 

18.  East  and  West  Section  through  the  Berlin  Porphyry,           -  250 

19.  North  and  South  Section  through  Pine  Bluff, 251 

20.  Ripple-Marked  Outlier,  Waterloo, 253 

21.  Profile  Section  Showing  the  Relations  of  the  Waterloo  Quartzite,        -        -  254 

22.  North  and  South  Section  through  Portland  Quartzite,          -  255 

23.  Section  Showing  the  Relations  of  the  Portland  Quartzite,    -  255 

24.  Section  of  Bartholomew's  Bluff, -        -  265 

25.  Section  Across  Green  Lake, 266 

26.  East  and  West  Section  near  Ripon, 270 

27.  Section  near  Stiles  Showing  Relations  of  St.  Peters  Sandstone  and  Lower 

Magnesian  Limestone. 271 

28.  Contact  of  Trenton  and  Lower  Magnesian  Limestones,        -        ...  273 

29.  North  and  South  Section  near  Ripon, 274 

30.  Irregular  Structure  of  Lower  Magnesian,  Nepeuskin,          ....  275 
bl.  Section  of  Lower  Magnesian  Limestone,    -------  278 

32.  Section  of  Lower  Magnesian  Limestone,  Mukwa, 279 

33.  Section  of  Lower  Magnesian  Limestone,  Mukwa, 279 

34.  Relations  of  the  Formations  in  the  Town  of  Ellington,        -        -        -        -  280 
85.  Coloration  of  the  St.  Peters  Sandstone  near  Ripon, 286 

36.  Coloration  of  the  St.  Peters  Sandstone  near  Ripon, 287 

37.  Relations  of  St.  Peters  Sandstone  and  Trenton  Limestone,  Magnolia,          -  289 

38.  Subdivisions  of  Trenton  Limestone, 291 

39.  Profile  of  Trenton  Limestone  near  Beloit, 297 

40.  Section  through  the  Iron  Ore  Deposit,  Iron  Ridge,      -  329 

41.  Section  at  the  Mayville  Ore  Bed,        -                330 

42.  Position  and  Relations  of  the  Iron  Ore  at  Hartford,     -----  333 

43.  Cascade  Falls  near  De  Pere, 333 

45.  Peculiar  Structure  of  Racine  Beds,  Germantown, 364 

46.  Stratification  at  Moody 's  Quarry, 365 

47.  Relation  of  the  Mound  and  Horizontal  Limestone,  Wauwatosa,  -  366 

48.  Profile  of  Leperditia  Beds  near  Waubakee,         ------  392 


REPORT  ON  CENTRAL  WISCONSIN. 

1.  Specimen  showing  junction  of  Potsdam  Sandstone  and  Archaean  Schists,  -    462 

2.  Vicinity  of  Point  Bass,  Wood  County, 466 

3.  Section  Across  Side  Channel  of  Wisconsin  River,  near  Point  Bass,           -  -    467 

4.  Section  Across  Side  Channel  of  Wisconsin  River,  near  Point  Bass,      -        -  467 

Wis.  SUB.— B 


xviii  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

Page. 

5.  Vicinity  of  Grand  Rapids,      -        - 470 

6.  Kaolin  at  Grand  Rapids,  471 

7.  Junction  of  Granite  and  Hornblende  Rocks. 473 

8.  Enlargement  of  a  portion  of  Fig.  7,  473 

9.  Granite  Vein  at  Grand  Rapids, 47-4 

10.  Granite  Vein  in  Gneiss  at  Grand  Rapids,   -  475 

11.  Generalized  Section,  Grand  Rapids, -  476 

12.  Map  of  Localities  at  Conant's  and  Stevens  Point  Rapids,    -  478 

13.  Sketch  of  Granite  Exposures,                                                   ....  479 
14   Granite  Vein  at  Conant's  Rapids, 480 

15.  Quartzite  Exposure  on  Rib  Hill,  Marathon  County,        -        -  -  485 

16.  Map  of  Rock  Exposures  near  Wausau,  4^6 

17.  Block  Vein  in  Syenite,  Wausau,     - 487 

18.  Rock  Occurrences  at  the  Falls  of  Rib  River, 489 

19.  Faulted  Veins  in  Granite,  Yellow  River, 492 

20.  Unconforniability,  Black  River  Falls,  493 

23.  Sketch  of  Original  Structure  and  Erosion  of  Baraboo  Ranges,        ...  5C6 

24.  Surface  of  Quartzite  Showing  Curved  Lamination, 509 

25.  Slaty  Cleavage  in  Quartz  Slate  at  Devil's  Lake, 510 

26.  Potsdam  Bowlder-conglomerate  and  Sandstone  on  Archaean  Quartzite  at  Devils 

Lake,  -        -        -  510 

27.  Sandstone  and  Conglomerate  on  Quartzite  at  Dorward's  Glen,   -        -        -  511 

28.  Unconforniability,  Sec.  23,  Caledonia, 512 

29.  Map  of  the  Lower  Narrows  of  the  Baraboo, 513 

30.  Section  through  West  Bluff  of  the  Lower  Narrows, 514 

31.  Upper  Narrows  of  the  Baraboo,  515 

32.  North  and  South  Section.  Upper  Narrows  of  the  Baraboo,       -        ...  516 

33.  Veined  Quartzite,      -----------  516 

34.  Sketch  of  Possible  Relations  of  Formations  near  Baraboo  Ranges,          -        -  539 

35.  Outlines  of  Roche  a  Cris  and  Friendship  Mound,  as  seen  from  Pilot  Knob,  567 

36.  Shape  of  the  summit  of  Roche  a  Cris, 572 

37.  Diagram  showing  how  an  Area  of  a  Lower  Formation  may  be  Entirely  Sur- 

rounded by  a  Higher  One, 583 

38.  North  and  South  Section  in  Scott, 585 

39.  Profile  Section  across  the  Valley  of  the  Wisconsin  at  Portage,         ...  586 

40.  Section  at  Kmgsley's  Bluff,  Lodi,       ...  587 

41.  Section  across  Valley  of  Wisconsin  in  West  Point  and  Merrimac,    -  588 

42.  Sketch  of  the  Western  Face  of  Gibraltar  Bluff,  588 

43.  Section  of  Gibralter  Bluff, -.589 

44.  Section  across  the  Valley  of  the  Wisconsin  in  Caledonia,    -        -        -        -  589 

45.  Section  across  the  Valley  of  the  Wisconsin  at  Prairie  du  Sac,          ...  591 

46.  Section  across  the  Wisconsin  Valley  from  Honey  Creek  Bluff,     -        -  591 

47.  Section  of  River  Bluff,  north  of  Spring  Green,  -  592 

48.  Map  and  Section  showing  the  Relations  of  Eiky's  Limestone,     -        -        -  593 

49.  Map  and  Section  showing  the  Relation  of  Outcrop  at  Wood's,        -        -        -  595 

50.  Section  in  town  of  Burke,  601 

51.  Section  across  the  Valley  of  the  Black  Earth  Creek, 607 

52.  Outline  of  an  Area  of  Trenton  Limestone  near  Columbus,  -  614 


TABLE  OF  CONTEXTS.  xix 
REPORT  ON  THE  LEAD  REGION. 

.Page 

1.  General  section  of  Platte  River  Valley,  -     6->7 

2.  Sketch  of  the  upper  part  of  the  Blue  Mounds,        -  659 

3.  Sketch  cf  the  Platte  Mounds,    -  -     661 

4.  Sketch  of  a  Terraced  Hill  near  Lumberville,  669 

5.  Section  of  Calcareous  and  Arenaoeous  Shales  at  Grant  River,  -      678 

6.  Section  of  Curved  Strata  at  Grant  River,    -  674 

7.  Sketch  of  Lower  Magnesian  Limestone  at  Welsh  Mill,  -      674 

8.  Sketch  of  a  Hill  in  the  Town  of  Mt.  Pleasant,        -  676 

9.  Upheaval  of  St.  Peters  Sandstone  at  Red  Rock,  -      678 

10.  Section  from  Scale's  Mound  to  the  State  Line.      -  686 

11.  Section  of  Openings  (ideal),       -  690 

12.  Plan  of  Workings  in  the  Beetown  Mine,     -  696 

13.  Junction  of  E.  and  W.  Veins  with  a  Quartering  Range,  Adkinson  Diggings,     698 

14.  Section  of  Meredith  Mine,  -  699 

15.  Section  of  Vein,  Black  &  Co.'s  Diggings,  -     703 

16.  Section  of  an  Opening  in  the  Williams  Mine  -                        703 

17.  Vein-stone  Breccia,  Stopline  Diggings,  -      714 

18.  Section  of  the  Barton  Opening,       -  718 

19.  Section  showing  Connection  of  Flat  and  Pitching  Sheets,  Linden  Mine          -      728 

20.  Section  of  Sheets  in  the  Road  Mine,  728 

21.  Plan  of  Evan  Williams'  Diggings,       -  -      730 


PAET  I. 


HISTORICAL. 


ANNUAL    REPORTS. 


PREFATORY  TOTE. 

The  administration  of  the  survey,  at  its  commencement,  was  placed 
in  the  charge  of  the  late  lamented  Dr.  I.  A.  Lapham,  who  brought 
to  the  work  the  fruits  of  a  large  experience,  and  the  acquisitions  of 
years  of  industrious  observation  upon  the  geology  and  natural  history 
of  the  state.  Under  his  able  management,  the  survey  continued  the 
first  and  the  greater  portion  of  the  second  year.  Annual  reports  for 
each  of  these  years  were  duly  submitted  by  him,  but  were  not  pub- 
lished. He  was  succeeded  as  chfef  geologist  in  February,  1875,  by 
Dr.  O.  "W".  Wight,  who  held  the  position  one  year,  and  who  presented 
a  report  for  that  year,  which  was  likewise  not  published.  In  Febru- 
ary j  1876,  the  direction  of  the  survey  was  placed  in  charge  of  the 
writer.  Subsequently,  provision  was  made,  by  enactment  of  the  legis- 
lature, for  the  preparation  and  publication  of  the  final  report  of  the 
survey,  and  the  foregoing  annual  reports  were  placed  "  in  the  hands  of 
the  chief  geologist  to  be  used  in  the  preparation  of  his  final  report." 
Under  these  circumstances,  it  has  seemsd  to  me  the  part  of  justice  to 
publish,  as  nearly  intact  as  possible,  the  reports  prepared  by  my  pre- 
decessors. Certain  portions  of  a  report  of  progress,  however,  necessa- 
rily relate  to  the  administration  of  the  survey,  and  to  other  matters 
of  transient  interest  which  have  little  subsequent  importance,  and 
would  be  inappropriate  in  a  report  of  this  character,  and  hence  there 
arose  a  necessity  for  the  revision  of  these  reports  for  this  volume. 
This,  to  me  a  very  delicate  duty,  it  was  presumed  would  be  esteemed 
a  favor  by  those  most  intimately  concerned  in  their  publication,  and 
it  was  freely  proffered  them.  The  revisal  of  the  reports  of  Dr.  Lap- 
ham  was  very  kindly  undertaken  by  his  son,  Mr.  S.  G.  Lapham,  and 
they  appear  as  they  left  his  hands,  with  a  few  trivial  changes  made  at 
his  request.  It  should  be  considered  by  all,  that  these  annual  reports 
made  thus  early  in  the  history  of  the  work,  and  merely  intended  to 
ehow  the  progress  and  results  of  the  survey,  in  accordance  with  legal 
requirement,  cannot  do  full  justice  to  their  distinguished  author,  but 
it  is  hoped  that  they  will  indicate  the  work  accomplished  under  his 
administration,  and  if  there  be  anything  meritorious  in  the  final 


4:  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

results  of  the  survey,  a  just  and  generous  public  will  award  a  due 
measure  of  honor  to  the  hand  that  organized  and  gave  it  direction  at 
its  inception. 

The  like  comity  in  relation  to  the  revision  of  the  report  of  1875, 
extended  to  Dr.  Wight,  \vas  declined,  except  the  privilege  of  reading 
the  proofs,  but  he  has  been  kind  enough  to  assure  me  that  nothing  has 
been  omitted  from  his  report  that  it  is  desirable  to  retain. 

The  revision  of  all  these  reports  has  been  closely  confined  to  the 
elimination  of  administrative  and  duplicate  portions,  and  everything 
of  a  geological  nature  has  been  retained,  even  though  it  were  only 
provisional  in  character,  and  this  has  been  done  to  the  exclusion  of 
portions  of  my  own  and  of  my  associates'  manuscript.  While  pub- 
lishing thus  fully  and  scrupulously  the  reports  of  my  predecessors,  it 
is  but  just  to  myself  to  disclaim  any  responsibility  for  the  views  pre- 
sented. 

Since  these  reports,  besides  being  themselves  the  earlier  annals  of 
the  survey,  contain  historical  sketches,  they  are  grouped  together  to 
form  the  opening  historical  section  of  the  volume. 

The  annual  report  for  1876,  submitted  by  the  writer,  was  promptly 
published,  and  hence  no  part  of  it  will  find  a  place  in  this  volume. 

The  annual  reports  of  the  assistant  geologists,  being  their  own  in- 
dependent productions,  were  placed  in  their  hands,  and  will  be  found 
incorporated  in  their  reports  upon  the  districts  assigned  them. 

T.  C.  C. 

BELOIT,  August  6,  1877. 


WISCONSIN  GEOLOGICAL   SURVEY. 


EEPOET  OF  PKOGBESS  AND  RESULTS, 

FOR  THE  YEAR  1873. 


BY  I.   A.   LAPHAM. 


As  required  by  the  act  "  to  provide  for  a  complete  geological  sur- 
vey of  Wisconsin,"  approved  March  19,  1873,  I  now  have  the  honor 
to  report  the  progress  made,  and  the  results  attained  during  the  first 
year  of  the  survey,  and  also  to  lay  before  you  the  maps,  profiles  and 
drawings  necessary  to  exemplify  the  same.  The  law  reads  as  follows : 

AN  ACT  to  provide  for  a  complete  Geological  Survey  of  Wisconsin. 
The  people  of  the  State  of  Wisconsin,  represented  in  Senate  and  Assembly  do  enact  as 
follows. 

SECTION  1.  The  governor  is  hereby  required  to  appoint,  by  and  with  the  advice  and 
consent  of  the  senate,  a  chief  geologist,  who  shall  be  a  person  of  known  integrity,  thor- 
ough practical  and  scientific  knowledge  of  the  sciences  of  geology  and  mineralogy,  and, 
upon  recommendation  of  said  chief  geologist,  the  governor  shall  appoint  one  or  more 
assistants,  not  exceeding  in  number  four,  one  of  whom  shall  be  a  skillful  analytical  chemist 
and  assayer;  the  said  chief  geologist  and  his  assistants  to  constitute  a  geological  corps, 
whose  duty  it  shall  be  to  make  a  thorough  and  complete  geological,  mineralogies!  and 
agricultural  survey  of  the  state,  and  topographical  surveys  of  such  portions  as  may  be 
deemed  by  the  corps  to  need  them  for  the  thorough  completion  of  the  work:  Provided, 
That  if  the  appointment  of  chief  geologist  be  made  during  the  recess  of  the  senate, 
such  appointment  may  be  confirmed  at  the  next  session  thereof. 

SECTION  2.    The  survey  shall  have  for  its  objects: 

1st.  An  examination  of  the  geological  structure  of  the  state,  including  the  dip,  num- 
ber, nmgnitude,  order  and  relative  position  of  the  various  strata;  their  richness  in  mine- 
rals, metallic  ores,  clays,  mineral  waters,  fertilizers,  building  stones  and  other  useful 
materials,  the  value  of  such  materials  for  economic  purposes,  and  their  accessibility  for 
mining  and  manufacture. 


6  GEOLOGICAL  SURVEY  OP  WISCONSIN. 

2d.  Accurate  chemical  analyses  and  assays  of  the  various  ores,  clays,  peats,  marls, 
building  stones,  etc.,  discovered  by  the  state. 

3d.  A  careful  topographical  survey  of  the  lead  region,  for  the  purpose  of  ascertaining 
as  far  as  possible,  the  amount  of  denudation,  and  the  exact  position  of  the  mining 
ground  at  each  locality;  also  careful  barometrical  observations  on  the  relative  elevation 
and  depression  of  various  parts  of  the  state. 

4th.  An  examination  of  soils  and  subsoils,  and  observations  upon  the  animal  and  vege- 
table productions  of  the  state,  with  reference  to  its  agricultural  interests. 

SECTION  3.  It  shall  be  the  duty  of  said  geological  corps,  in  the  progress  of  the  ex- 
aminations hereby  directed,  to  collect  such  specimens  of  rocks,  ores,  fossils,  minerals,  etc., 
as  may  be  necessary  to  exemplify  the  geology  of  the  state.  Sets  of  these  specimens  shall 
be  deposited  with  the  "Wisconsin  Academy  of  Sciences,  Arts  and  Letters,  and  the  State 
University,  and  with  each  one  of  the  incorporated  colleges  of  the  state,  and  with  each 
of  the  normal  schools :  provided,  application  be  made  to  the  chief  geologist  before  the 
commencement  of  field  work. 

SECTION  4.  It  shall  be  the  duty  of  the  chief  geologist  and  his  assistants,  on  or  before 
the  first  Monday  in  January  in  each  year  during  the  continuation  of  the  survey,  to  mako 
to  the  governor  a  report  of  the  progress  and  results  of  the  survey,  accompanied  by  such 
maps,  profiles  and  drawings  as  may  be  necessary  to  exemplify  the  same,  which  reports 
the  governor  shall  lay  before  the  legislature. 

SECTION  5.  As  soon  as  the  progress  of  the  survey  will  permit,  the  chief  geologist  shall 
begin,  and  on  completion  of  the  survey,  shall  complete  a  final  report,  including  the  re- 
sults of  the  entire  survey,  accompanied  by  such  drawings  and  topographical  maps  as 
may  be  necessary  to  illustrate  the  same,  and  by  a  single  geographical  map  showing  by 
colors  and  other  appropriate  means  the  stratification  of  rocks,  the  localities  of  the  beds 
of  mineral  deposits,  and  the  character  and  extent  of  the  different  formations. 

SECTION  6.  To  carry  into  effect  the  provisions  of  this  act,  the  sum  of  thirteen  thou- 
sand dollars  for  each  year,  until  the  completion  of  said  survey,  is  hereby  appropriated 
to  be  drawn  from  the  treasury  on  wa.rrants  from  the  governor,  as  needed;  which  shall 
be  in  full  for  all  expenditures  except  printing  of  reports.  The  salary  of  the  chief  geolo- 
gist, and  the  salaries  of  the  assistant  geologists  shall  be  fixed  by  the  governor,  and  shall 
be  for  services  actually  performed,  and  time  actually  spent  in  the  work.  The  balanco 
of  the  sum  hereinbefore  appropriated  shall  be  used  in  such  manner  as  shall  best  pro- 
mote the  purposes  of  this  act. 

SECTION  7.  The  survey  shall  commence  by  the  first  of  June  next,  or  as  soon  thereaf- 
ter as  practicable,  beginning  with  the  counties  of  Ashland  and  Douglas,  and  the  entire 
survey  shall  be  completed  within  four  years  from  and  after  its  commencement. 

Approved  March  19,  1873. 

ORGANIZATION  or  THE  GEOLOGICAL  CORPS.  —  Governor  0.  C.  Wash- 
bum,  by  commission  dated  the  tenth  day  of  April,  1873,  appointed 
the  undersigned  chief  geologist  under  the  provisions  of  this  law. 

On  the  twenty-ninth  day  of  the  same  month,  Prof.  Roland  D.  Irv- 
ing, A.  M.,  E.  M.,  Prof.  T.  C.  Chamberlin,  A.  M.,  and  Mr.  Moses 
Strong,  A.  M.,  were  upon  the  recommendation  of  the  chief  geologist 
appointed  as  assistants  in  the  survey.  Prof.  "W.  W.  Daniells,  M.  S., 
was  also  engaged  to  make  such  chemical  examinations  and  analyses 
of  ores  and  minerals  as  might  be  needed  for  the  -survey.  By  an  ar-- 
rangement  with  the  Regents  of  the  State  University,  Prof.  Darnells 


ANNUAL  REPORT  FOR  1873.  7 

is  to  have  the  use  of  the  apparatus  belonging  to  the  Institution  with- 
out additional  expense. 

These  gentlemen  had,  by  previous  study  and  training,  qualified 
themselves  for  the  special  work  required.  Their  elaborate  reports 
herewith  submitted  will  show  that  they  have  faithfully,  efficiently, 
and  satisfactorily  performed  the  several  duties  assigned  them ;  though 
the  time  between  the  close  of  the  field  operations  and  the  day  on 
•which  their  reports  must  be  submitted  to  the  Governor  is  not  suffi- 
cient to  enable  them  to  do  that  full  justice  to  their  work  that  could 
be  desired. 

The  assistants  were  each  directed  to  organize  a  party  adequate  to 
the  special  work  required;  to  supply  themselves  with  the  necessary 
instruments  and  outfit;  to  give  their  attention  to  all  facts  throwing 
light  upon  any  of  the  special  matters  required  to  be  considered  by  the 
law  authorizing  the  survey;  and,  as  it  is  obviously  impossible,  as  well 
as  unnecessary  to  visit  every  square  mile  in  the  country  they  were 
directed  to  so  plan  their  routes  as  to  be  able  to  examine  the  localities 
of  greatest  importance  to  the  material  interests  of  the  state;  and  at 
the  close  of  the  fieldwork,  to  prepare,  as  soon  as  possible,  a  detailed 
report  of  the  results  of  their  work  with  the  necessary  maps,  profiles 
and  drawings.  Each  party  was  supplied  with  skeleton  maps,  traced 
from  the  township  plats  of  the  government  land  surveys,  upon  which 
was  laid  down,  from  time  to  time,  such  additional  information  as 
could  be  obtained.  These  plats,  it  is  well  known  represent  "  town- 
chips  "  six  miles  square,  divided  into  thirty-six  "  sections  "  of  one  mile 
square,  upon  a  scale  of  two  inches  to  one  mile,  which  is  sufficiently 
large  to  represent  all  but  the  minutest  details  of  the  geological  sur- 
vey. Among  the  instruments  brought  into  requisition  by  the  sever- 
al parties  wrere  the  aneroid  barometer,  miners'  compass,  odometer, 
clinometer,  pocket  level,  tape  lines,  etc. 

PROF.  IRVMG'S  PARTY.  —  It  was  deemed  advisable  to  assign  to 
Prof.  Irving  of  the  State  University,  Madison,  the  duty  of  beginning 
the  survey,  by  an  examination  of  the  Iron  and  Copper  Ranges  of 
Ashland  and  Douglas  counties ;  and  efforts  were  made  to  have  the 
work  begun  as  soon  after  the  first  day  of  June  as  possible.  His  party, 
consisting  of  Prof.  R.  D.  Irving,  Mr.  Frank  B.  Jenney,  Mr.  Edmund 
T.  Sweet,  and  Mr.  James  Munro,  with  a  guide  and  a  cook,  though 
much  delayed  by  ice  in  Lake  Superior,  were  able  to  reach  .Ashland, 
and  to  commence  the  field-work  of  the  "Wisconsin  Geological  Survey 
on  Monday  the  second  day  of  June,  A.  D.  1873. 

In  addition  to  the  general  instructions  detailed  above,  Prof.  Irving 


8  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

was  requested  to  give  attention  to  the  question  of  the  age  of  the  red 
saudstone  and  accompanying  shale  of  the  counties  to  be  examined; 
whether  the  Archaean  rocks  are  of  different  ages;  and  to  the  disturb- 
ances of  the  strata  in  the  vicinity  of  the  metal-bearing  ranges,  involv- 
ing important  questions  regarding  the  proper  system  of  mining. 

His  report,  herewith  submitted,  will  be  found  to  contain  ample  de- 
tails of  the  beds  of  silicious  magnetic  iron  ores  forming  what  is 
known  as  the  Penokee  Iron  Range,  with  numerous  analyses  of  the 
ores,  including  all  information  necessary  for  a  proper  understanding 
of  the  extent  and  value  of  these  important  ore  beds.  Other  details 
brought  forward  in  this  report,  showing  what  had  previously  been 
done  in  exploring  this  interesting  region;  its  topography,  surface, 
general,  special  and  economical  geology;  its  agricultural  features, 
timber,  etc.,  will  be  found  equally  interesting  and  valuable.  These 
explorations,  made  so  early  in  the  season,  were  not  accomplished  with- 
out the  patient  endurance  of  much  suffering  and  hardship,  arising 
from  the  clouds  of  musquitoes,  and  from  unfavorable  weather. 

Prof.  Irving  also  made  a  partial  examination  of  the  iron  ore  beds 
at  and  near  the  Black  Kiver  Falls,  in  Jackson  county. 

PROF.  CHAMBEKLIN'S  PAKTY.  —  To  Prof.  Chamberlin  was  assigned 
the  duty  of  surveying  that  portion  of  the  state  lying  immediately 
west  of  the  line  of  outcrop  of  the  Niagara  or  Clinton  group  of  rocks, 
from  the  south  line  of  the  state  through  the  counties  of  "Walworth, 
Jefferson,  Dodge,  Fond  du  Lac,  Calumet  and  Outgamie  to  the  south- 
ern limits  of  the  crystalline  Archaean  rocks  in  Shawano  county;  and 
upon  his  return  route,  to  examine  the  outcrops  of  the  lower  strata  lying 
west  of  that  line.  He  would  thus  be  led  to  examine  the  important 
iron  beds,  now  so  extensively  mined  at  Iron  Bidge,  the  artesian  wells 
from  which  water  flows  so  abundantly  at  Fond  du  Lac  and  elsewhere, 
and  the  highly  interesting  localities  of  quartzite  in  Dodge  and  Jeffer- 
son counties.  He  would  also  be  in  the  midst  of  some  of  the  most 
striking  features  of  the  glacial  and  modified  "  drift,"  with  their  "  pot- 
ash kettles,"  gravel  hills  and  parallel  ridges. 

On  the  twenty-third  day  of  June,  work  was  commenced  by  this 
party  under  the  immediate  direction  of  Prof.  Chamberlin,  aided  dur- 
ing portions  of  the  time  by  Messrs.  L.  C.  Wooster,  F.  H.  King,  jN". 
D.  "Wright,  Samuel  Shaw  and  G.  L.  Merriman. 

They  reached  Keshena,  in  Shawano  county,  early  in  September,  and 
returned  to  Beloit  by  the  last  of  that  month.  Some  further  explora 
tiona  were  afterwards  made  by  Prof.  Chamberlin  in  person,  as  men- 
tioned in  his  report. 


ANNUAL  REPORT  FOR  1873.  9 

In  Prof.  Cliamberlin's  report  will  be  found  much  interesting  and 
valuable  information,  stated  in  plain  language,  relating  to  the  topog- 
raphy of  the  district  examined  by  him ;  the  drainage  and  water  power; 
the  distribution  of  vegetation,  of  marshes,  of  lands  covered  with  oak, 
maple  or  pine  forests,  with  a  map  showing  the  boundaries  of  these 
several  divisions;  the  outlines  of  the  several  rock  formations;  the 
phenomena  of  the  drift;  the  nature  of  artesian  wells,  and  various 
matters  coming  under  the  head  of  economical  geology.  Special  at- 
tention was,  very  properly,  given  to  the  subject  of  our  peat  deposits, 
which  will  increase  in  importance  from  year  to  year,  as  the  forests 
disappear,  and  the  cost  of  fuel  becomes  thereby  increased. 

These,  and  the  various  other  matters  of  much  practical  utility  pre- 
sented in  this  report,  will  be  read  with  much  interest  by  the  people 
of  the  state. 

MB.  STRONG'S  PAKTT.  —  Special  provision  having  been  made  for  a 
careful  topographical  survey  of  the  lead  region,  for  the  purpose  of 
showing  the  denudation  of  the  superior  strata  that  so  evidently  has 
occurred,  and  the  exact  position  of  the  mining  ground  at  each  locality, 
with  reference  to  the  particular  rock-formation  in  which  it  is  found, 
it  was  deemed  advisable  to  assign  one  of  the  three  surveying  parties 
expressly  to  this  work.  Accordingly  Mr.  Strong,  having  made  suita- 
ble preparations,  commenced  that  work  on  the  fifth  day  of  June. 

For  the  purpose  of  securing  the  most  general  and  complete  view  of 
the  whole  lead  region  during  the  first  year  of  the  survey,  Mr.  Strong- 
was  directed  to  give  his  attention  to  two  lines,  the  one  east  and  west,  the 
other  north  and  south  through  the  middle  of  the  district.  This  wTould 
lead  him  to  construct  a  geological  section  from  the  Mississippi  river 
eastward  to  Dane  and  Green  counties,  and  another  northward  from 
the  state  line  of  Illinois,  to  the  iron  ores  and  quartzites  of  Richland 
and  Sauk  counties.  This  party  consisted  of  Mr.  Moses  Strong,  Mr. 
A.  D.  Conover,  and  Mr.  J.  "W.  T.  Crawford.  Mr.  Strong's  previous 
training  and  skill  acquired  in  the  best  scientific  schools  in  this  country 
and  in  Germany,  and  in  the  business  of  a  mining  engineer,  enabled 
him  to  perform,  with  full  satisfaction,  the  duties  thus  assigned  to  him. 

Special  attention  was  to  be  given  to  the  collection  of  all  facts  bear- 
ing upon  the  method  by  which  the  lead,  zinc,  and  copper,  were  depos- 
ited in  the  veins  or  crevices;  whether  by  deposition  from  above, 
injection  from  below,  or  by  gradual  infiltration  from  the  inclosing 
rocks ;  these  questions  being  deemed  of  the  greatest'  theoretical  and 
practical  importance  as  showing  the  probable  extent  of  these  ores  be- 
low the  limits  of  present  explorations.  Also  to  ascertain  whether 


10  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

there  have  been  disturbances  of  the  strata,  centers  of  elevation,  etc., 
questions  of  importance  with  regard  to  the  downward  continuance  oi! 
the  veins,  and  the  proper  method  of  drainage. 

Mr.  Strong's  report  will  be  found  to  contain  much  that  is  new  and 
valuable  in  regard  to  this  important  and  very  interesting  district. 
The  local  details,  showing  the  present  condition  of  the  mines,  and 
their  capabilities  of  future  production,  cannot  fail  to  be  of  great  bene- 
fit to  the  state  by  making  known  in  a  reliable  form  the  advantages 
that  might  be  attained  by  a  more  vigorous  prosecution  of  mining 
operations  at  many  of  the  localities  described. 

The  extent,  physical  characteristics,  mineral  contents,  and  other 
important  particulars  of  each  rock-formation  occurring  in  the  district 
examined,  are  clearly  stated.  The  discovery  of  fossils  in  the  Lower 
Magnesian  limestone  shows  that  animal  life  was  not  entirely  destroyed 
during  the  epoch  of  the  deposition  of  this  great  member  of  the  Lower 
Silurian  series  of  rocks,  and  places  it  more  directly  in  unison  with  the 
Galena  (or  Lead-bearing)  limestone  from  which  it  is  only  separated  by 
a  comparatively  thin  layer  of  sandstone  —  the  St.  Peters.  It  thus 
being  shown  to  have  one  more  character  in  common  with  that  rock, 
we  may  expect  to  find  still  more  common  features,  such  as  the  occur- 
rence of  crevices,  openings,  and  the  ores  of  lead,  zinc,  and  copper. 
Important  facts  are  brought  forward,  bearing  upon  this  question  of 
the  occurrence  of  metallic  ores  of  economical  value,  in  the  Lower 
Magnesian  limestone. 

Quarries  of  brown  sandstone  equal  in  beauty  and  value,  and  possess- 
ing in  many  respects  the  same  qualities,  with  that  so  much  admired 
from  Lake  Superior,  are  first  publicly  noticed  in  this  report. 

Prominence  is  also  very  properly  given  to  the  layers  of  carbona- 
ceous shale,  containing  from  fifteen  to  forty-five  per  cent,  of  bitumin- 
ous matter,  which  may,  at  some  future  time,  be  utilized  in  some  way. 
It  was  found  that  this  shale  occupies  a  position  between  the  Blue 
limestone  below,  and  the  Galena  limestone  above;  and  it  thus  be- 
comes a  ready  means  of  determining  the  exact  position  of  the  mining 
grounds,  with  reference  to  the  geological  formations.  We  have  here 
probable  evidence  of  a  considerable  period  of  time  during  which  vege- 
table life  —  perhaps  in  the  form  of  sea  weeds  —  predominated,  and 
which  may  be  regarded  as  an  incipient  effort  towards  the  state  of 
things  that  long  ages  afterwards  supplied  coal  and  oil  to  the  world. 
'  The  history  of  former  efforts  in  the  production  of  copper  at  Mineral 
Point  will  be  found  interesting,  and  may  lead  to  renewed  efforts  in 
that  direction. 

"With  regard  to  the  zinc  ores  —  consisting  of  the  sulphuret  (sphaler- 


ANNUAL  REPORT  FOR  1873.  11 

ite  or  blende)  and  the  carbonate  (Smithsonite,  or  dry-bone)  often, 
though  improperly,  called  calamine,  a  term  rightfully  belonging  to 
the  silicious  oxide,  that  probably  does  not  occur  in  the  lead  region  — 
full  details  will  be  found  in  Mr.  Strong's  report,  showing  the  wonder- 
ful increase  of  production  within  the  past  two  or  three  years.  We 
have  here  a  case  where  an  ore,  supposed  for  a  long  time  to  be  worth- 
less, is  suddenly  invested  with  great  value;  and  owners  of  abandoned 
mines,  find  themselves  in  the  possession  of  unexpected  wealth.  It  is 
to  be  regretted  that  the  want  of  a  cheap  fuel  in  the  lead  region  pre- 
vents the  smelting  of  these  ores  within  our  own  state.  The  construc- 
tion of  a  railroad  from  Milwaukee  directly  to  the  source  of  supply  of 
these  zinc  ores,  by  cheapening  the  cost  of  transportation,  might  render 
the  manufacture  of  spelter  and  zinc- white,  a  business  of  profit  on  the 
shores  of  Lake  Michigan. 

It  is  proper  here  to  call  attention  to  the  fact  that  Wisconsin  lead  i« 
known  in  the  arts  as  soft  lead,  in  centra-distinction  from  hard  lead, 
so  called,  that  comes  from  the  far  west.  The  latter  kind,  separated 
mostly  from  the  silver  lead  ores,  is  supposed  to  contain  other  metals 
as  impurities ;  while  the  former  is  free  from  all  deleterious  substances. 
Doubtless  the  poisonous  quality  of  some  lead  pipes  used  for  the  con- 
veyance of  water  may  arise  from  the  presence  of  arsenic,  or  other  im- 
purities from  which  our  lead  is  free. 

The  very  extended  series  of  barometrical  observations  for  altitude, 
made  by  Mr.  Strong  and  his  party,  will  have  special  value  in  the 
mining  region,  not  only  at  present  but  for  all  future  time. 

Another  highly  important  subject,  the  diminution  of  the  flow  of 
water  from  springs,  and  in  the  rivers  and  smaller  streams  is  very 
properly  presented,  and  many  new  facts  mentioned.  Although  this 
falling  off  of  the  amount  of  water  may  be  an  advantage  in  working 
the  lead,  zinc  and  copper  mines,  allowing  the  miner  to  penetrate  to 
greater  depths  before  the  steam  pump  or  the  tunnel  must  be  resorted 
to,  yet  in  view  of  other  vital  interests,  this  drying  up  of  the  living 
waters  is  to  be  deemed  a  disaster,  which  it  should  be  the  business  of 
a  wise  and  prudent  government  to  check.  Within  the  life-time  of  an 
individual,  perhaps  the  change  is  not  sufficient  to  be  of  much  conse- 
quence; but  within  the  life  of  the  state,  it  will  become  a  matter 
deserving  the  most  serious  attention. 

It  is  perhaps  to  be  regretted,  that  the  necessity  of  extending  the 
geological  survey  over  the  whole  state,  with  an  area  of  fifty-six  thou- 
sand square  miles,  renders  it  impossible  to  make  such  special  surveys 
of  each  mining  district  as  are  wanted  for  the  practical  purposes  of  the 
miner,  and  seem  to  be  expected  in  some  localities.  Such  working 


12  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

plans  can  only  be  made  by  the  mining  companies,  and  landed  propri- 
etors. Had  this  work  been  undertaken  for  each  mining  neighborhood, 
there  would  have  been  but  little  time  or  means  left  for  the  prosecu- 
tion of  the  survey  in  other  portions  of  the  state. 

It  is  deemed  to  be  the  proper  business  of  the  state  survey  to  ascer- 
tain the  dip,  number,  magnitude,  and  relative  position  of  the  various 
rock-strata;  and,  in  the  lead  region  especially,  to  make  a  careful  top- 
ographical survey  for  the  purpose  of  ascertaining  as  far  as  possible 
the  amount  of  denudation,  and  the  exact  position  of  the  mining 
ground  at  each  locality.  The  miner  is  thus  supplied  with  correct  and 
tangible  information  to  guide  him  in  conducting  his  operations  in 
prospecting  for  new  ranges,  by  showing  which  are  the  mineral-bear- 
ing rocks,  with  their  locality,  dip,  and  thickness.  This  must  be  done, 
not  only  for  the  mining  region  proper,  but  for  the  whole  state. 

It  is  the  proper  business  of  the  miner,  at  the  expense  of  the  owners, 
and  not  of  the  geologist  at  the  public  expense,  to  search  with  pick  in 
hand,  within  the  limits  thus  denned,  for  mineral  ranges,  sinking 
shafts  here  and  there  until  he  meets  with  success.  It  then,  and  not 
until  then,  becomes  the  business  of  the  mining  engineer  to  make  those 
minute  and  detailed  investigations  and  surveys  that  are  needed  in  tho 
preparation  of  working  plans,  maps  and  profiles,  showing  the  most 
proper  and  economical  method  of  working  the  mines  so  discovered. 
Such  survey  and  map  should  show  the  exact  extent,  location,  and  dip 
of  the  several  veins,  with  their  crossings;  the  present  condition  of  the 
works ;  the  proper  system  of  drainage ;  the  depth  to  which  the  veins 
maybe  supposed  to  extend;  the  contour  of  the  ground;  and  many 
other  items,  varying,  of  course,  with  the  peculiarities  of  each  location. 

Such  surveys  and  plans  are  necessary  for  the  proper  working  of  any 
mines,  as  has  often  been  found  at  great  cost;  but  they  do  not  come 
within  the  requirements  of  the  law  authorizing  and  defining  the  pres- 
ent geological  survey  of  Wisconsin.  Should  such  surveys  ever  be 
undertaken  by  the  state,  the  work  now  being  done  by  Mr.  Strong, 
will  be  a  necessary  preparation  for  their  proper  execution. 

To  indicate  what  is  required  by  owners  of  mining  property  in  the 
lead  region.  Mr.  Strong  has  prepared  a  map  of  the  Blue  Mounds  in 
Dane  and  Iowa  counties,  with  the  Brigham  mines,  showing  the  geo- 
logical formations  in  colors,  in  the  usual  method,  and  also  the  topog- 
raphy by  contour  lines,  and  the  depth  at  which  each  rock  would  be 
reached  from  any  point.  With  the  accompanying  explanations  it  will 
be  found  that  this  kind  of  map  shows  a  very  considerable  amount  of 
special  information  needed  for  practical  purposes,  and  for  deciding 
many  important  questions  in  regard  to  the  proper  working  of  the  mines. 


ANNUAL  REPORT  FOR  1873.  13 

To  Mr.  James  "Wilson,  Jr.,  of  Cassville,  the  survey  is  indebted  for 
R  traced  copy  of  his  detailed  and  very  valuable  working  map  of  the 
Muscalunge  diggings  in  Grant  county,  showing  in  full  detail  the  ex- 
act location,  direction,  and  extent  of  all  the  drifts,  adits,  and  shafts, 
with  the  depth  of  the  principal  shafts,  and  the  local  names  by  which 
they  are  known.  This  map  will  be  of  general  interest  as  showing  the 
intricate  and  complicated  nature  of  these  drifts  in  the  lead  region.  It 
could  only  be  constructed  from  surveys  made  at  different  times  dur- 
ing the  history  of  mining  operations;  for  many  of  these  drifts  and 
shafts,  having  been  abandoned,  are  now  obstructed  with  rubbish  or 
filled  with  water.  To  explore  and  survey  them  at  this  time  would 
require  a  heavy  outlay  in  clearing  these  passages;  an  outlay  which 
would  scarcely  be  justified,  except  for  the  purposes  of  the  owner  in 
recommencing  the  work  of  mining. 

The  experience  gained  during  the  past  year  will  perhaps  enable  us 
to  do  a  greater  amount  of  work  hereafter.  Much  of  the  detailed  in- 
formation collected  does  not  properly  come  into  a  report  intended 
more  especially  to  show  the  progress  of  the  work,  and  to  give  early 
notice  of  important  discoveries.  Our  note  books  will  again  be  called 
into  service  in  the  preparation  of  the  final  report,  intended  to  em- 
brace the  whole  subject. 

PRACTICAL  IMPORTANCE  OF  GEOLOGICAL  KNOWLEDGE.  —  The  propri- 
ety of  a  more  general  diffusion  of  accurate  knowledge  of  the  simplest 
facts  and  deductions  in  modern  geological  science  is  evinced  by  the 
very  positive  assurances  of  numerous  letter  writers  that  coal  is  found 
—  having  been  dug  out  by  badgers,  or  otherwise  exposed  —  in  this 
state,  which  is  well  known  to  be  entirely  underlaid  by  strata  of  date 
much  older  than  the  coal-formation.  We  found  one  party  diligently 
boring  into  a  stratum  of  soft  green  shale,  just  like  —  as  he  informed 
us  —  the  clay  under  which  coal  is  found  in  Ohio  and  Pennsylvania. 
The  slightest  examination  of  the  fossils  found  in  this  shale  sufficed 
to  show  that  it  belonged  to  the  Silurian  age,  and  was  deposited 
long  before  those  peculiar  conditions  were  brought  into  existence, 
which  gave  origin  to  the  coal.  "We  had  here  a  practical  illustra- 
tion of  the  importance  of  the  study  of  paleontology,  the  index, 
by  means  of  which  any  given  formation  wherever  found,  can  at 
once  be  referred  to  its  proper  position  in  the  geological  series,  and 
thus  lead  with  unerring  certainty  to  inferences  of  the  greatest  practi- 
cal importance. 

Other  parties  were  found  sinking  shafts,  or  digging  wells  under  the 
direction  of  "  spiritual  mediums,"  or  of  persons  skilled  with  the  di- 


34: 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


vinmg  rod.     Such  persons  can  seldom  be  convinced  of  the  futility  of 
their  labor  by  an  appeal  to  the  fossils. 

ME.  EDGERTON'S  SURVEY.  —  Mr.  B.  II.  Edgerton,  engineer,  having 
been  commissioned  by  the  Milwaukee  and  Northern  Railroad  Com- 
pany to  survey  the  northern  extension  of  their  road  from  Green  Bay, 
an  arrangement  was  made  with  him  to  report  the  results  of  such  ob- 
servations as  he  might  be  able  to  make,  that  would  forward  the  ob- 
jects of  the  geological  survey.  The  line  run  was  from  near  Green 
Bay,  in  ranges  19  and  20,  very  directly  north  to  the  Menomonee  river, 
which  it  crossed  at  the  head  of  the  Big  Quinnesec  Falls.  The  list  of 
elevations  furnished  by  him  shows  the  height  of  the  ground  above 
the  level  of  Lake  Michigan  at  the  crossing  of  every  section  line,  and 
the  level  of  the  surface  of  the  water  in  the  rivers  over  which  the  line 
was  run.  These  latter  are  as  follows: 


Sec. 

T. 

R. 

ELEVATION  ABOVE 

Lake 
Michigan. 

The  Sea. 

Littl6  Suamico  

26 
35 
23 
25 
1 
24 
36 
25 
24 
31 
13 
26 
18 
5 
21 
15 
33 
10 
7 
18 

26 
27 
27 
28 
28 
29 
30 
30 
30 
31 
31 
32 
33 
33 
34 
35 
37 
37 
38 
38 

East. 
19 
19 
19 
19 
19 
19 
19 
19 
19 
19 
19 
19 
20 
20 
20 
20 
20 
20 
20 
20 

Feet. 
144 
128 
139 
132 
164 
180 
157 
157 
159 
135 
139 
162 
192 
211 
242 
309 
415 
438 
472 
571 

Feet. 
722 
706 
717 
710 
742 
758 
735 
735 
737 
713 
717 
740 
770 
789 
820 
887 
993 
1,01  C 
1,050 
1,149 

North  branch  of  Pensaukee  

Oconto  above  the  falls  

North  branch  of  Littl6  riv6r  

Little  Pt'shtisro        

Little  Poshtigo  lake  

A  small  lake  on  

Beaver  creek  on  

Peshtigo  river  

Middle  inlet     

North  branch  

AVausaukan  river  

Pike  river  

Peminee-Bon-AVon  river  

North  branch  of  same  

Menomonee  river  

Highest  ground  (2  miles  south  of  river) 

No  indications  of  the  existence  of  workable  beds  or  veins  of  iron 
ore  were  observed  upon  this  route;  if  any  exist  they  are  further  to 
the  north  and  west. 

Mr.  Edgerton  reports  as  follows:  "The  geological  formation  of  the 
country  traversed  I  found  to  be  much  the  same  as  indicated  on  your 
map,  except  that  I  did  not  succeed  is  discovering  any  evidence  of  the 
belt  marked  thereon  as  the  St.  Peters  sandstone.  The  first  cropping 


ANNUAL  REPORT  FOR  1873.  15 

out  of  the  rock  which  we  found  is  at  the  Oconto  Falls,  in  section  25, 
town  28,  range  19  east,  where  the  Magnesian  limestone  makes  its 
appearance  in  the  banks  of  the  river  and  adjacent  bluffs.  The  per- 
pendicular fall  here  is  about  twenty-two  feet,  and  the  rapids  which 
succeed  make  the  whole  fall  of  the  river  about  sixty  feet. 

"We  first  discovered  the  Potsdam  sandstone  in  section  34,  town 

31,  range  19,  where  the  bed  and  banks  of  a  small  creek  are  of  this 
formation.     It  is  a  dark-colored  loose  stone,  too  soft  to  serve  any  use- 
ful purpose.     At  the  falls  of  the  Peshtigo  river,  in  section  24,  town 

32,  range  19,  this  sandstone  is  of  a  firmer  and  finer  texture,  and  may 
be  found  useful  as  a  building  material.     It  has  also  a  sharp  grit,  and 
close  grain,  that  renders  it  serviceable  for  grindstones,  and  I  was  told 
that  at  an  early  day  it  was  used  for  sharpening  edged  tools. 

"In  section  36,  town  33,  range  19,  granite  first  shows  itself,  and 
with  other  metamorphic  rocks,  crops  out  from  time  to  time  until  we 
reach  the  Menomonee  river.  It  is  a  very  abundant  material  at  Pike 
river,  in  sections  15  and  16,  town  35,  range  20,  and  forms  the  bed 
and  banks  of  the  river  at  the  falls.  In  section  34,  town  37,  range 
20,  trap  rocks1  are  found  interspersed  with  the  granite,  along  the 
banks  of  the  Peminee-Bon-Won,  but  after  leaving  that  stream  until 
we  reach  the  north  branch  in  section  3  of  the  same  township,  no  rocks 
appear  on  the  surface  except  granite.  At  the  crossing  of  the  North 
Branch,  trap  rocks  again  make  their  appearance  and  are  frequently 
seen  in  alternation  with  the  granite,  until  we  reach  the  crossing  of  the 
Menomonee  river  on  section  7,  town  38,  range  20,  at  the  head  of  the 
Big  Quinnesec  Falls;  at  which  point  the  rocks  are  mostly  granite,  but 
a  small  area  at  the  top  is  composed  of  trap  mingled  with  some  talcose 
rocks. 

'"The  granite  of  this  region  is  mostly  schistose  in  character  and  is 
frequently  coarse  and  soft,  so  as  to  be  of  little  use  as  a  building  ma- 
terial. It  often  abounds  in  seams,  filled  with  feldspar,  and  other  sub- 
stances; and  quite  frequently  these  seams  cross  each  other  at  acute 
angles. 

"From  the  Peshtigo  river  I  went  westward  as  far  as  Thunder  Lake, 
in  section  15,  town  32,  range  18,  and  first  discovered  the  granite  in 
this  direction  near  the  line  between  ranges  18  and  19,  and  at  the 
point  between  sections  13  and  18. 

"At  Keshena  in  town  27,  range  15,  or  a  little  northwest  from  the 
village,  the  same  rocks  appear;  and  I  judge  that  the  line  between  the 
sandstone  and  granite  follows  about  a  northeasterly  course  to  the  Me- 
nomonee river,  in  town  36,  range  21  east/' 

1  These  and  the  following  rocks  spoken  of  as  trappean  are  metamorphic 


16  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

TOPOGRAPHICAL  SURVEY.  —  Much  of  the  success  of  any  geological 
survey  depends  upon  the  accurate  measurement  of  the  elevation  of 
the  country  above  some  well  known  datum  plane.  For  all  such  deter- 
minations in  Wisconsin  the  level  of  Lake  Michigan  forms  a  conven- 
ient base  from  which  to  measure.  The  elevation  of  this  lake  above 
the  sea  was  long  ago  determined,  by  the  topographer  of  the  early 
Michigan  geological  survey,  under  the  direction  of  the  lamented  Dr. 
Douglas  Houghton,  to  be  578  feet.  Probably  the  first  spirit  level 
brought  to  "Wisconsin  was  that  of  the  late  Hon.  Byron  Kilbourn,  who 
in  March,  1836,  established  the  zero,  at  the  lake  level,  to  which  all 
subsequent  work  of  street  grading,  sewers,  and  the  water-works  of 
Milwaukee  has  been  referred.  It  was  also  from  this  now  well  es- 
tablished datum  plane  that  the  surveys  of  the  Milwaukee  &  Missis- 
sippi, the  La  Crosse  &  Milwaukee,  and  the  Milwaukee  &  Horicon 
railroads  were  commenced;  and  it  is  to  this  zero  therefore,  that  all 
work  of  the  present  geological  survey  will  be  referred. 

Since  1836,  the  level  of  Lake  Michigan  has  varied,  from  4  feet  above 
this  datum,  in  July,  1838,  to  1.65  below  in  March,  1848,  showing  a 
total  change  of  5.65  feet;  the  mean  being  about  one  foot  above  the 
established  zero. 

These  fluctuations  have  long  been  known  to  result  from  various 
causes,  among  them  the  effect  of  winds  and  storms;  the  annual  change 
of  the  seasons  producing  high  and  low  water,  as  in  ordinary  rivers ; 
the  variations,  during  different  years,  or  series  of  years,  as  to  wetness 
or  dryness;  and  finally  a  regular  (though  very  small)  lunar  tide,  cor- 
responding with  that  of  the  ocean. 

RAILROAD  ELEVATIONS.  —  In  the  prosecution  of  any  topographical 
as  well  as  of  any  other  survey  of  the  state,  it  is  apparent  that  advant- 
age should  be  taken  of  any  work  already  done  by  others;  and  with 
this  view,  efforts  have  been  made  to  secure,  as  far  as  can  now  be  done 
the  results  of  the  several  railroad  surveys  within  the  state,  and  the 
following  list  of  stations,  with  their  elevation  above  Lake  Michigan 
and  the  sea  will  show  what  progress  has  been  made  in  this  direction. 

Every  railroad  station,  the  elevation  of  which  is  here  given,  becomes 
a  bench  mark  from  which  our  barometrical  measurements  of  the  rela- 
tive elevation  and  depression  of  various  parts  of  the  state,  as  well  as 
all  future  surveys  can  be  made,  with  definite  knowledge  of  the  abso- 
lute height  above  Lake  Michigan  and  above  the  sea  level. 

The  level  of  Lake  Michigan,  thus  definitely  made  known,  will  be 
found  a  convenient  datum  plane  to  which  all  future  railroad  surveys 
may  be  referred;  this  can  be  done  without  the  use  of  negative  quan- 


ANNUAL  REPORT  FOR  1873. 


17 


titles,  for  no  part  of  Wisconsin  lies  below  that  level.  After  the  pub- 
lication of  the  following  list,  it  will  not  be  difficult  to  connect  any 
future  survey  with  this,  now  well  established  datum  plane,  and  thus 
aid  directly  in  the  development  of  the  physical  geography  and  topo- 
graphy of  the  state. 

ELEVATION  OF  RAILROAD  STATIONS. 


STATIONS. 

COUNTY. 

ELEVATION  ABOVE 

Lake 

Michigan. 

The 
Sea. 

Sauk  

301 

480 
180 
293 
466 
553 
128 
145 
154 
426 
645 
395 
117 
560 
389 
174 
284 
320 
379 
340 
409 
153 
163 
248 
184 
232 
302 
231 
304 
85 
379 
89 
158 
421 
47 
191 
220 
246 
400 
85 
203 
299 
284 
356 
246 
234 
...  362 
191 

879 
1053 
758 
871 
1044 
1131 
706 
723 
732 
1001 
1223 
973 
695 
1138 
967 
752 
862 
898 
957 
918 
987 
781 
741 
826 
762 
810 
880 
800 
882 
608 
957 
667 
736 
1000 
625 
769 
798 
824 
978 
663 
781 
877 
8C2 
9:3-4 
824 
812 
940 
709 

Ackerville          

\Vashington  

Afton                                  .  .   .  . 

Rock  

Walworth  

Amlierst    

Portage  

Portage  

Appleton     

Outagamie  (C  &  N  W  )  

Appleton  

Outagamie  (M.  &N)  

Iowa  

Arlin°'ton    

Columbia  

Wood  

Augusta  

Eau  Claire  

Iowa  

Baldwin    

St.  Croix  

Wood  

La  Crosse  

Baraboo    

Sauk  ,  

Barton  

^Vashington  

Juneau  

Beaver  Dam  

Dodge  

Bearse  Marsh.  

Wood  

Belgium  

Ozaukee  

Beloit    

Rock  

Bellville  

Jefferson  

Green  Lake  • 

BlackEarth    

Dane  

Black  River  •  

Jackson  

Black  River  Falls 

Jackson  

Blooms      .  . 

Sauk  

Blue  River  

Grant  

Boardman  
Boscobel    •  '   

St.  Croix  
Grant  

Branch-Zalesburg  

Manitowoc  

Brandon  

Fond  du  Lac  

Bridgeport  .       

Crawford  

Bristol  

Kenosha  

Brodhead  

Green  

Brookfield  Junction  

^Vaukesha  

Brooklyn  

Green  

Brown  Deer  

Milwaukee  
Racine  

Burnett  Junction  

Dodge   

Columbia    .  .     .  • 

Camp  Dou°°las  Junction  ....... 

Juneau  

Cato  °.  

Manitowoc  

Calamine  ...<  

La  Fayette  

Calvary  

Fond  du  Lac  

Cedarburg  

Ozaukee  

Wis.  SUK.—  2 

18 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 
ELEVATION  OP  RAILROAD  STATIONS  —  continued. 


STATIONS. 

COUNTY. 

ELEVATION  ABOVE 

Lake 
Michigan. 

The 

Sea. 

Cedar  Creek,  Ackerville  

TVashington  

480 
114 
431 
945 
269 
363 
330 
775 
256 
117 
280 
481 
367 
224 
305 
179 
341 
356 
9 
417 
107 
691 
838 
234 
154 
160 
360 
390 
365 
360 
268 
266 
242 
93 
297 
362 
413 
351 
170 
166 
388 
325 
487 
357 
290 
283 
168 
2)38 
240 
250 
220 
6 
305 
200 
150 
206 
325 

1058 
692 
1009 
1523 
846 
941 
908 
1353 
834 
695 
858 
1059 
945 
802 
873 
757 
919 
934 
587 
995 
685 
1269 
1416 
812 
732 
738 
933 
968 
943 
938 
846 
844 
820 
671 
875 
940 
991 
929 
748 
744 
966 
903 
1065 
868 
935 
861 
746 
816 
818 
828 
798 
584 
883 
778 
728 
784 
903 

Cedar  Grove  

Sheboygan   

Centralism  

Wood  

Chippewa  

Chilton  

Calumet  

Rock  

Clyman  

Dodge  

Colby  

Columbus  

Columbia  

Cross  Plains  

Dane  

Dane    

Dane  

La  Fayette  

Deanville  

Dane  ...»  

Decca  

Sheboygan  

De  Forest  

Delavan  

TVaJworth  

Dexterville  

Wood  

Dillman  

Milwaukee  

Dodgev  11°  

Iowa  

Dorchester  

Chippewa  

Dover  

Racine  

Dreuckers  

Calumet  «•  

Doyles  —  Otsego  

Columbia  >••  

Devils  Lake  

Sauk  

Eagle  

\Vaukesha  

Dane  

Eau  Claire  

Eau  Claire  

Rock    

Ehiers  Crossing  
Eldorado  

Ozaukee  
Sheboygan  

Elkhart  Lake  

Sheboycpcin  

Elkhorn  

Elk  Mound 

Elm  Grove          •       

\Vaukesha  

Elm  Grove  

^V^aukesha  

Elrov  .  . 

Rock  

Fairchild     

Eau  Claire  

Fall  Creek  

Eau  Claire  

Fall  River    

Columbia  

Fayette    .   ..       

"\V  alworth  

Fond  du  Lac  

Fond  du  Lac  

Footville       •       .       

Rock  

Forest  House  

^W^aukesha  

Forest  Junction  

Calumet  

Jefferson  

Fort  Howard  

Brown   

Dodge  

Fox  River  

Kenosha  
Racine  

Ozaukee  

Genesee  .. 

Waukesha  

ANNUAL  REPORT  FOR  1873. 
ELEVATION  OP  RAILROAD  STATIONS  —  continued. 


19 


STATIONS. 

COUNTY. 

ELEVATION  ABOVE 

Lake 
Michigan. 

The  Sea. 

WalwoHh  

274 
264 
285 
297 
183 
353 
289 
419 
112 
170 
448 
168 
205 
6 
365 
471 
235 
141 
525 
209 
408 
333 
210 
240 
588 
190 
250 
364 
306 
211 
128 
354 
418 
61 
345 
240 
221 
193 
243 
335 
572 
240 
.  80 
40 
101 
333 
315 
10 
286 
349 
547 
249 
70 
303 
154 
292 
250 

852 
842 
863 
895 
761 
931 
867 
997 
690 
748 
926 
740 
783 
584 
943 
1048 
813 
719 
1108 
787 
986 
911 
798 
818 
1166 
768 
828 
942 
884 
789 
706 
932 
996 
639 
923 
818 
799 
771 
821 
913 
1150 
818 
658 
618 
679 
911 
893 
588 
864 
927 
1125 
827 
648 
881 
732 
870 
8v>S 

^Valworth  

Giffords         

AVaukesha  

Monroe       .  .       .             .  • 

Sheboygan  

Monroe  

Milwaukee  ,  

Ozaukee  

Wood  

Milwaukee  

La  Fayette  

Brown  

Gr66n  Bcty  Jet  (Mcrrillcin)  .   ... 

Jackson  

Monroe  

Green  Lake  

Brown  

Hammond  

St.  Croix  
Rock  

Hartland       

^^aukoshci  

Columbia  

Calumet  

St  Croix  

Monroe  

Hilbert         

Calumet  

Monroe  

Dodge  

Jefferson  

St  Croix  

Sheboyg'an  

Clark  

Milwaukee  

Dodge  

Rock  

Jefferson  

Jefferson  

Green  

Portage  . 

Racine  

Outaganiie  

Kenoslia  

Kenosha  

Kiel     

Calumet  ; 

Columbia  

Milwaukee  

Sauk  

Marathon  

Koshkoiiong  

Rock  

La  Crosse  

La  Fayette  

Monroe  

Lake  

Milwaukee  

Like  Side  

\Vaukeslia  

Launartine  .  . 

Fond  du  Lac  .  . 

20 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 
ELEVATION  OP  RAILROAD  STATIONS  —  continued. 


ELEVATIO 

S     ABOVE 

STATIONS. 

COUNTY. 

Lake 
Michigan. 

The 
Sea. 

Latham  

Calumet  

143 

721 

La  Salle  

Sauk  •.  

320 

898 

Led°>eville  

Brown  . 

96 

674 

Lemonweir  

Juneau  

316 

894 

Le  Roy    

Monroe 

375 

953 

Lewiston  

Columbia  

231 

809 

Lima  

Rock  

310 

888 

Linden        

Juneau  .  .   .  . 

820 

898 

Lindwerrn  

Milwaukee   

56 

634 

Little  Chute       

Outagamie        .  .  . 

144 

722 

Lisbon  

Juneau  

315 

893 

Lone  Rock  

Richland  

126 

704 

Lodi     ,  

Columbia  

271 

849 

Dodge  

247 

825 

Monroe  

389 

967 

Lyons  •  - 

"Walworth  

222 

800 

Madison  east  

Dane  

268 

846 

Dane  . 

275 

853 

Magnoh'a    

Rock  

340 

918 

Manawa  

W'aupaca  

246 

824 

Manitowoc  

7 

585 

Marathon  

713 

1291 

Marshall   •  

Dane  

286 

864 

Juneau  

309 

887 

Dane  

195 

773 

McFarland           •       •       

Dane  

289 

867 

Medford     

Chippewa  

842 

119A 

Medina   '  

Outagamie  

192 

77(> 

Menasha  

Wlnnpba.°'o    . 

177 

755 

Dunn  

306 

884 

Merrillan  

Jackson  

365 

943 

Merrimac  

Sauk  

219 

797 

0/aukee  

92 

670 

Middleton  

Dane  

347 

925 

Mill  Creek  

Wood  

514 

1092 

Milton  

Rock  

293 

871 

Milton  Junction  

Rock  

299 

877 

Milwaukee    

Milwaukee  

5 

583 

Mineral  Point    

Iowa  

357 

935 

Minnesota  Junction  

Dodge  

348 

926 

Monroe  

Green  

492 

870 

Morrison  ..-  

Dane   

387 

965 

109 

687 

Nashotah  

W"aukesha  

350 

928 

Neenah  

^Vinnebti°'0  

170 

748 

Nepeuskin  (Rush  Lake  Junction) 

Wlnnebago    

263 

841 

New  Holstein  

Calumet   ..  .  .  .   .  . 

351 

929 

New  Richmond  
Northport  

Sb.  Croix  
W'aupaca  

411 

182 

989 
760 

North  Prairie  

^^aukesha    

363 

941 

North  Wisconsin  Junction  
Norway  

St.  Croix  
Monroe  

295 
407 

872 
985 

Oak  Creek  

Milwaukee  

86 

664 

Oakfield  

Fond  du  Lie  

310 

888 

Oakwood    

Milwaukee  

105 

685 

Oconomowoc  

W^aukesha  

283 

861 

Osrdensbure1   . 

WauDaca.  . 

292 

870 

ANNUAL  REPORT  FOR  1873. 
ELEVATION  OF  RAILROAD  STATIONS  —  continued. 


21 


STATIONS. 

COUNTIES. 

ELEVATION   ABOVE 

Lake 
Michigan. 

The 
Sea. 

Okee  

Columbia   

220 
102 
327 
365 
313 
170 
360 
205 
260 
232 
713 
263 
350 
119 
504 
262 
232 
388 
87 
41 
188 
428 
40 
43 
5 
378 
295 
155 
800 
407 
242 
403 
381 
352 
352 
208 
462 
61 
363 
313 
304 
259 
440 
403 
562 
263 
331 
171 
198 
275 
181 
365 
474 
66 
386 
7 
H5 

798 
680 
905 
943 
891 
748 
938 
783 
838 
810 
1291 
841 
928 
697 
1082 
840 
810 
966 
665 
619 
766 
1006 
618 
621 
583 
956 
873 
733 
878 
985 
820 
981 
959 
930 
930 
786 
1040 
639 
941 
891 
882 
837 
1018 
981 
1140 
841 
909 
749 
776 
853 
759 
943 
1052 
644 
964 
585 
fifiR 

Ozaukee  *  

Juneau    

Ore°°on  

Dane  ....   

Orf  ord                  .'  

Rock                                

Oslikosh  

\Vinneba°'o    

Otsego  

Columbia  

Pacific  .         .           

Palmyra  

Jefferson  *  

Pardeeville  •'  

Columbia  t  

Penokee  Gap  

Ashland  

Pewaukee  

Pins  Lake  

^Vaukesha 

Pleasant  Prairie  

Kenosha     •  .         • 

Plover  

Portage  

Plymouth  

Sheboygan 

Columbia  

Port  Edwards  .  ~  f  .  . 

Wood  

Port  Washington  

Ozaukeo  

Prairie  du  Chien  

Crawford  .... 

Princeton  

Green  Lake  .  . 

Rablin  

Wood  

Racine  (C.  &  N.  W.)  

Racine  

Racine  Junction  

Racine  .    ... 

Racine  (W.  U.)  

Racine  

Randolph  

Random  Lake  

Sheboygan  ..... 

Readstown  

\remon 

Reedsburg  ... 

Sauk  

Reeds  Corners  „  

Fond  du  Lac  • 

Reedville  

Remington  

Wood  . 

Richfield  

\Vashington.  . 

Rio  

Fond  du  Lac 

Riverside  

La  Fayette  .    .     . 

Roberts   

St   Croix  

Rockland  

Brown   

Rolling  Prairie  

Dodge  

Rosendale  

Fond  du  Lac  •   •  • 

Rosendale  (west)  

Fond  du  Lac  

Royalton  

TiVaupaca    .  • 

Rubicon  

Dodge  

Rudds  

Rudolph  

Wood  . 

Rush  Lake  Junction  

W^innebago  

Rusk  

Dunn  

Salem  

La  Crosse 

Salem  

Kenosha     • 

Sanderson  

Dane  

Saukville  

Ozaukee  

Scandinavia  , 

\Vaupaca  

Schleisingerville  

\Vashington 

Schwartzburg  Junction  

Milwaukee  

Scranton  

Jackson  

Sheboygan  

Sheboygan 

Sheboygan  Falls  .  . 

Shebovsran  .  . 

22 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 
ELEVATION  OP  RAILROAD  STATIONS  —  continued. 


STATIONS. 

COUNTIES. 

ELEVATION  ABOVE 

Lake 
Michigan. 

The 

Sea. 

Sherwood  

Calumet  

253 
366 
215 
730 
248 
270 
144 
90 
90 
475 
349 
508 
65 
279 
398 
356 
320 
173 
88 
383 
295 
101 
483 
273 
117 
182 
366 

354 

254 
241 
243 
448 
474 
225 
345 
314 
314 
643 
73 
60 
115 
923 
275 
144 
359 
183 
73 
241 
518 
102 
414 
304 
179 
86 
333 
373 

831 
944 
793 
1308 
826 
848 
722 
668 
668 
1053 
927 
1086 
643 
857 
976 
934 
908 
751 
666 
961 
873 
679 
1061 
851 
695 
760 
944 

932 

832 
819 
821 
1026 
1052 
803 
923 
892 
892 
1221 
651 
638 
693 
1501 
853 
722 
917 
761 
651 
819 
1096 
780 
992 
882 
757 
664 
911 
ciM 

Rock  

Sparta  

Monroe    

Spencer  

Marathon  

Spring  Creek  

Calumet  ...       .... 

Springfield.   ». 

^^al  worth  

Sauk  

State  Line  

Racine  C  &  N  W  

Racine,  C    M  &  St  P  

State  Line  

La  Fayette  

St  Cloud  

Sheboygan    

Portage  

St  Francis    

Milwaukee  

Dane  

Fond  du  Lac  

Sun  Prairie  •  

Dane  

Dane  

Taycheedah  

Fond  du  Lac  

Thienville  

Ozaukee  

Tomah      

Troy  Center  

^^alworth  

Tunnel  City  (Greenfield)   

Monroe  

Turtle  Creek  

Rock  

UUao  

Racine  

TJnion  Center  

Juneau  

Valley  Junction,  Wis.  Val-  [ 
ley  R.  R.  &  W.  W.  R.  R.  \'  ' 
Waldo  

Monroe  

Shehoy^an  <  

^Vaterloo  ••• 

Jefferson  

"Watertown  Junction  

Jeflerson  

^Vaukau    

^Vinnebago  

V^aunakee  

Dane  

W  aupun  

Dodge  

Marathon   

Milwaukee  

Crawford  

YV  pedens  Crossing  

Sheboygan  

"^"estboro    

Dane  .  •  

Racine  

^Vestport  

Dane  

\V  eyauweg  a  

W  aupaca  

White  Fish  Bay  

Milwaukee  . 

Wliitewater  

W^alworth  

Wilson  
Wilson  

St.  Croix  
Sheboygan   

Wilton  

"Windsor  

Dane  

La  Crosse    .... 

^Tonewoc   

Juneau  

Woodland.  .  . 

Dod^e  .  . 

ANNUAL  REPORT  FOR  1873. 
ELEVATION  OF  RAILROAD  STATIONS  —  continued. 


23 


STATIONS. 

COUNTIES. 

ELEVATION  ABOVE 

Lake 
Michigan. 

The 
Sea. 

\Voodnicin    

73 
170 
1038 
353 
48 
249 
158 

651 

748 
1616 
931 
626 
827 
736 

Wood  worth  
Worcester  

Kunosha  

Jackson  

\Vrightstown  ••  

^VVocena      .       »»   

Columbia.  

Sjalesbursr  

Manitowoc  

ELEVATION  OF  LAKES  IN  WISCONSIN. 


Dodffs   •  

282 
200 
269 
288 
390 
270 
362 
305 
324 
300 
235 
620 
325 
277 
376 
260 
184 
273 
951 
739 
270 

860 
778 
847 
866 
968 
848 
940 
883 
902 
878 
813 
1198 
903 
855 
954 
762 
851 
838 
1529 
1317 
848 
578 
840 
906 
769 
882 
868 
867 
860 
841 
994 
838 
784 
873 
841 
799 
856 
783 
600 
1539 
1028 
839 
7G8 
740 

Vi^ciukcslici  

Sauk  

VlWiorf  ffttaiirm^ 

Sli6boyffcin  

-Dodg"6   

TK-ft-V)                                      

PnnpTrc*  f~R    T?    Rridflrel 

"Walworth  ••••   

Polk  

Dodf'e  

Dane   

Jefferson  ••  

T  a  "Rpllp 

TV^aukcsha  

Oconto  

Bayfield  

Mpnrlnfn    (4.fM 

262 
328 
191 
304 
290 
289 
282 
263 
416 
260 
206 
295 
263 
221 
278 
205 
22 
961 
450 
261 
190 
162 

llnd 

\Vaukeslia  

PilrP 

Kenosha   

Green  Lake  

\V^innebago  

Cilvpr                                               

Waukesha  

Winhpssa   (9(1} 

Dane  

WinrJ 

Racine  

^V^iunebago  

GEOLOGICAL  SURVEY  OF  WISCONSIN. 
ELEVATION  OF  SUMMITS,  MOUNDS,  HIGHLANDS,  ETC. 


ELEVATION  ABOVE 

Lake 
Michigan. 

The  Sea. 

State  Line  of  Illinois  — 

262 
349 
90 
475 
1150 
674 
607 
443 
1151 
1000 
703 
591 
462 
713 
669 
824 
555 
605 

840 
927 
668 
1053 
1728 
1252 
1185 
1021 
1729 
1578 
1281 
1169 
1040 
1291 
1247 
1402 
1133 
1183 

"  C.  &  N.  W.  R.  R.  (Sharon)  
"        "C    M  &  St  P  

St  Croix  and  Brule  Portage  (Ow6n)  «  

Mount  Trenipealeau  (Owen)  -  ......... 

"West  Blue  Mound  CW  hitney)  

En  st  Blue  Mound  (^Tiitney)       

Platte  Mound  (at  base  553)  

Sinsinewa  Mound  College  

Government  Hill  (\Vaukcsha  Co  )  

Elephants  Back  (Kilbourn  City  

Buena  Vista  Sec  23  T  22  R  9  E  

GOVEKNMENT  SURVEYS. — It  is  very  generally  known  that  the  admi- 
rable system  of  surveys  into  townships,  six  miles  square  and  sections 
of  one  mile  square,  with  their  boundary  lines  running  due  north  and 
south  and  due  east  and  west,  adopted  for  the  survey  of  the  government 
lands  of  the  United  States,  though  exceedingly  well  adapted  to  the 
purposes  for  which  it  was  chiefly  intended,  that  of  disposing  of  these 
lands,  is  altogether  too  crude  and  inaccurate  for  any  scientific  purpose. 
There  are  offsets  occasioned  by  the  spheroidal  shape  of  the  earth,  that 
could  not  be  avoided,  but  there  are  also  many  other  irregularities  arising 
from  various  causes  which  prevent  the  construction,  from  these  surveys 
alone,  of  an  accurate  map  of  the  state.  Among  these  causes  may  be 
mentioned  the  necessity,  often  occurring,  for  making  surveys  of  public 
lands  to  meet  the  wants  of  settlement  and  improvement  before  the 
principal  or  governing  lines  can  be  run.  Some  townships  have  been 
resurveyed  in  a  neighboring  state,  revealing  gross  irregularities,  only 
to  be  accounted  for  by  a  want  of  honesty  on  the  part  of  the  surveyor; 
how  many  similar  cases  exist  in  Wisconsin  can  only  be  known  when 
the  country  becomes  fully  occupied,  and  the  lines  of  the  public  survey 
retraced. 

While  some  tiers  of  sections  are  double  the  usual  width  1  others  are 


In  range  9,  towns  21  to  30,  inclusive. 


AXXUAL  REPORT  FOR  1873.  25 

contracted  to  a  quarter  of  their  proper  size1.  Some  section  lines  in- 
stead of  running  due  east  and  west,  or  due  north  and  south,  are  found 
to  make  considerable  angles  with  these  cardinal  directions.  Almost 
every  section,  when  accurately  remeastired,  is  found  to  show  either  an 
excess  or  a  deficiency  of  the  normal  quantity  of  six  hundred  and  forty 
acres.  Railroad  engineers  discover  these  inaccuracies  while  running 
their  lines  with  the  theodolite,  and  connecting  them  with  the  section 
lines.  One  who,  under  instructions,  followed  a  section  line  over  a 
level  country,  was  afterwards  censured  for  the  curves  he  had  intro- 
duced at  almost  every  mile  of  the  road,  where  only  a  straight-line  was 
intended. 

On  the  official  plats  of  the  surveys  of  the  public  lands,  now  depos- 
ited in  the  office  of  the  secretary  of  state,  at  Madison,  we  often  find 
the  north  line  of  a  township  varying  considerably  from  the  true  east 
and  west  direction;  while  the  south  boundary  of  the  next  township 
(which  is  the  same  line)  shows  no  such  variation2.  Again,  the  east 
line  of  one  plat  differs  from  the  west  line  of  the  next  in  the  same 
manner.  In  all  such  cases  there  are  no  means,  short  of  actual  re- 
survey,  of  determining  which  is  correct,  nor  what  changes  are  required 
in  the  form  of  the  subdivisions,  or  the  direction  of  their  boundary 
lines,  to  make  them  conform  to  these  unexplained  irregularities. 

If  we  plat  one  of  the  banks  of  the  Mississippi  or  Menomonee  rivers 
by  the  Wisconsin  surveys,  and  the  other,  upon  the  same  map,  from 
those  of  Iowa  and  Minnesota,  or  of  Michigan,  we  shall  find  that  these 
rivers  have  in  some  places  a  wonderful  breadth,  while  at  others  the 
two  banks  will  be  brought  so  near  together  as  to  leave  scarcely  room 
for  a  trout  brook. 

Considerable  progress  has  already  been  made  in  an  attempt  to  trace 
all  these  irregularities;  to  show  the  offsets  upon  the  correction  lines, 
and  to  construct  a  diagram  or  skeleton  map  which  shall  correctly  rep- 
resent the  surface  of  the  state.  This  work  must  be  done  before  any 
correct  map  of  the  state  can  be  made.  Such  maps  are  found  to  be 
matters  of  necessity  in  all  civilized  countries;  large  amounts  of  money 
and  many  years  of  labor  having  been  expended  to  secure  this  object 
in  Great  Britain,  France,  and  many  other  countries. 

The  proper  corrections  to  be  made  in  the  lines  of  the  public  land 
surveys  can  only  be  ascertained  and  applied  after  a  complete  geodetic 
survey  shall  be  made,  such  as  is  now  being  prosecuted  by  the  general 
government,  under  the  direction  of  the  coast  survey  and  of  the  engi- 
neer department.  Such  survey  contemplates  the  accurate  determina- 
tion of  the  latitude  and  longitude  of  numerous  prominent  points 

1  In  town  16,  range  1  to  11  east.  *  Notably  townships  1  and  2  in  range  9  east. 


26  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

which  are  to  be  connected,  and  made  the  basis  of  a  system  of  triangu- 
lation,  covering  all  the  ground  to  be  surveyed. 

The  engineer  department  of  the  United  States  army  have  in  charge 
the  survey  of  the  lakes,  which  reaches  into  this  state  along  the  shores 
of  Lake  Superior,  Lake  Michigan  and  Green  Bay,  and  also  other  mili- 
tary and  geographical  surveys  in  the  west.  The  work  of  the  lake  sur- 
vey will  be  available,  so  far  as  it  goes,  for  the  purposes  of  the  state 
survey,  and  it  is  exceedingly  desirable  that  it  should  be  extended  so  as 
to  embrace  a  larger  portion  of  the  interior.  At  my  suggestion  Gen. 
Humphrey,  chief  of  engineers,  has  authorized  the  determination  of 
the  position  of  points  on  the  base  line  of  the  land  survey  (the  south- 
ern boundary  of  the  state)  and  others  on  the  fourth  principal  meridi- 
an, and  on  the  "correction  lines;"  these  being  the  governing  lines 
of  the  public  land  surveys,  their  exact  determination  becomes  of  the 
greatest  importance.  Should  the  congressional  appropriation  for  these 
objects  be  continued,  other  work  of  the  same  kind  will  be  done. 

If  such  a  survey  could  be  extended  over  the  state  of  Wisconsin,  and 
properly  connected  with  the  land  surveys,  it  would  accomplish  all  that 
could  be  desired  in  this  direction.  It  was  found  that  congress,  while 
making  provision  for  extending  the  coast  survey  across  the  continent, 
so  as  to  form  a  geodetic  connection  between  the  Atlantic  and  Pacific 
coasts,  required  also  the  determination  of  points  in  each  state  in  the 
Union,  which  shall  make  requisite  provision  for  its  own  topographical 
and  geological  surveys.  Under  this  authority,  the  officers  of  the  coast 
survey  have  already  taken  observations  for  determining  the  position 
of  Madison  and  La  Crosse,  and  arrangements  have  been  made  for  the 
further  prosecution  of  the  work,  which  will  be  in  charge  of  Prof.  J. 
E.  Davies,  of  the  University  of  Wisconsin.  In  addition  to  the  general 
benefits  of  that  survey,  it  will  be  the  means  of  training  a  number  of 
young  men  in  the  methods  of  this  important  kind  of  work,  thus  mak- 
ing it  the  source  of  educational  advantages. 

Other  important  surveys  have  been  made  by  the  general  govern- 
ment within  our  state.  Among  them,  perhaps  the  most  valuable  are 
those  made  a  few  years  ago  under  the  direction  of  Gen.  G.  K.  Warren, 
of  several  of  the  larger  rivers,  including  the  Mississippi  so  far  as  it 
forms  our  western  boundary,  and  portions  of  the  St.  Croix,  Chippewn,, 
Black,  Wisconsin  and  Fox  rivers.  Of  these,  maps  were  constructed 
on  a  scale  of  two  inches  to  one  mile  (same  as  the  plats  of  the  govern- 
ment land  surveys),  showing  not  only  the  margins  of  the  rivers,  with 
the  islands  and  sand  bars,  but  also  the  boundaries  of  the  bottom  lands 
and  the  position  of  the  adjacent  bluffs.  Copies  of  these  detailed  and 
costly  maps  have  been1  furnished  for  the  use  of  the  state  survey,  and 


ANNUAL  REPORT  FOR  1873.  27 

add  very  materially  to  our  knowledge  of  the  minute  topography  of 
the  state.  They  will  also  soon  become  still  more  valuable  as  a  means 
of  showing  what  changes  are  annually  taking  place  along  the  course  of 
these  important  rivers. 

With  the  public  land  surveys,  thus  tested  and  corrected,  together 
with  the  railroad  surveys,  and  the  barometrical  measurements  of 
heights  by  the  geological  survey,  we  shall  have  abundant  material  for 
the  construction  of  a  very  full  and  correct  topograpical  map  of  the 
state. 

It  is  therefore  to  be  hoped  that  means  will  not  be  withheld  for  the 
vigorous  prosecution  of  these  important  surveys  on  the  part  of  the 
United  States  government.  All  such  work  is  of  the  greatest  practi- 
cal importance  in  the  more  correct  determination  of  the  boundaries 
of  real  estate,  thus,  perhaps,  preventing  future  litigation,  neighbor- 
hood quarrels,  and  uncertainty  as  to  the  ownership  of  property. 

MINERALS.  —  The  following  enumeration  of  the  mineral  species 
heretofore  found  in  Wisconsin,  has  been  made  up  from  observation, 
and  from  various  sources  of  information ;  and  though  it  is,  doubtless, 
far  from  complete,  either  in  the  number  of  species  existing  in  the 
state,  or  in  the  enumeration  of  localities,  it  will  serve  as  a  beginning 
towards  the  more  complete  mineralogical  survey  contemplated. 

CATALOGUE  OF  MINERALS.1 
I.  NATIVE  ELEMENTS. 

Gold.  —  Gold  is  said  to  have  been  found  in  several  places  in  the  northern  part  of  the  state. 

Silver.  —  Native  silver  is  found  associated  with  copper  in  boulders  of  the  drift,  having 
been  transported  from  the  copper  veins  of  Lake  Superior.  It  is  said  to  occur  in  veina 
on  the  Montreal  river;  and,  associated  with  lead,  in  Ashland  county. 

Copper.  —  Copper  has  been  found  in  limited  quantities  in  regular  veins  on  the  Montreal 
river  and  at  several  other  places  in  Ashland  and  Douglas  counties.  In  the  form  o£ 
drift  boulders  it  is  often  found,  especially  in  the  eastern  half  of  the  state;  the  masses 
vary  from  a  few  ounces  to  several  hundred  pounds;  the  largest,  found  near  Hustis- 
ford  in  Dodge  county,  had  a  weight  of  487  pounds. 

Iron,  —  Meteoric  iron  has  been  found  in  Washington  county  on  the  farm  of  Louis  Korb, 
in  masses  varying  from  8  to  62  pounds.  They  are,  apparently,  all  fragments  of  one 
meteorite  which  must  have  exploded  when  very  near  the  surface  of  the  ground.  It 
has  been  analyzed  and  described,  and  samples  sent  to  collectors  under  the  name  of 
the  "  "Wisconsin  Meteorite."  The  presence  of  nickel,  and  peculiar  Widmannstathiazi 
figures  leave  no  doubt  of  the  meteoric  origin  of  tin's  iron. 

Native  Sulphur.  —  Sulphur,  resulting  from  the  decomposition  of  marcasite,  has  been 
found  in  the  lead  mines  at  Mineral  Point,  Shullsburg,  etc. 

Graphite  (Plumbago,  Black  Lead).  —  Graphite  is  said  to  have  been  found  in  the  northern 
portion  of  the  state. 

i  A  list  of  all  the  minerals  known  at  the  close  o/the  survey  to  occur  in  the  state  will  be  given  ia 
another  volume  of  the  report. 


28      '  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

II.   SULPHIDS,   AlWENIDS,  ETC. 

Galenite  (Sulphuret  of  Lead).  —  Extensively  mined  in  the  southwestern  counties  of  the 

state.     Occurs  in  small  quantities  in  many  other  localities. 
Sphalerite  (Blende,  Blackjack).  —  Abundant  and  now  extensively  mined  in  the  lead 

region. 

Chalcocite  (Sulphuret  of  Copper).  —  At  Mineral  Point,  and  other  places. 
Niccolite  (Arsenical  Nickel).  —  Found  in  very  small  quantities  in  Douglas  county,  1873. 
Pyrite  (Cubical  Iron  Pyrites).  —  At  Mineral  Point,  etc. 
Chalcopyrite  (Copper  Ore).  —  At  Mineral  Point,  Mt.  Sterling  and  other  places,  but  not 

in  workable  quantity. 
Marcasite  (Iron  Pyrites,  Mundig). — With  ores  of  lead  and  zinc  in  the  lead  region; 

masses  in  drift  clay  near  Lake  Michigan,  and  elsewhere. 
Tetrahedrite  (Gray  Copper  Ore). —  Left  Hand  River,  Douglas  county.     (Owen.) 

III.  OXYGEN  COMPOUNDS. 

Cuprite  (Red  Copper  Ore).  —  Left  Hand  River,  Douglas  county.  (Dana.) 
Water.  Natural  waters  in  the  Archaean  and  Sandstone  regions  are  usually  soft  and  nearly 
pure;  in  other  portions  of  the  state,  hard,  or  containing  lime  and  magnesia  from  the 
limestones.  At  Sparta,  Waukesha,  etc.,  the  water  of  certain  springs  and  wells  is 
found  to  possess  medicinal  virtues.  At  Fond  du  Lac,  Sparta  and  Watertown,  the 
iron  tubes  through  which  the  water  flows  become  highly  magnetic. 

Hematite  (Red  and  Specular  Iron  Ore).  —  Iron  Ridge,  Hartford,  Depere,  etc.,  in  small 
grain;  flax  seed  ore.  Used  with  Lake  Superior  ores  at  Milwaukee  and  other  places. 
Penokee  Iron  Range,  Ashland  county,  Wood  county,  etc. 

Menaccanite  (Titanic  Iron  Ore).  —  In  email  quantities  near  Baraboo,  Sauk  county.  In 
trap  rocks,  Lake  Superior.  (Owen.) 

Magnetite  (Magnetic  Iron  Ore). — Penokee  Iron  Range,  Ashland  county,  in  great  abund- 
ance; also  at  Black  River  Falls,  Jackson  county,  and  other  places.  It  is  found  La 
the  form  of  sand  on  the  shores  of  the  great  lakes. 

Limonite  (Brown  Iron  Ore).  —  Ironton,  Sauk  county,  supplying  an  iron  furnace.  In  lees 
quantities  at  various  places,  resulting  from  the  decomposition  of  inarcasite.  Bog 
ore  in  Wood  county  and  elsewhere. 

Wad  (Oxide  of  Manganese).— In  small  quantities  in  the  lead  region,  and  other  places; 
also  the  variety  asbolite  or  earthy  cobalt. 

Quartz.  —  Crystalized  quartz  is  found  in  various  places.  In  the  form  of  grains  it  con- 
stitutes the  sandstones,  often  pure  and  white.  •  Its  varieties,  amethyst,  carnelian, 
jasper,  chert,  etc.,  are  often  found.  Quartzite  occurs  in  extensive  ridges  among  the 
Archaean  rocks. 

Amphibole  (Hornblende,  etc.). — Abundant  in  the  Archaean  rocks.  Variety,  tremolite  a,t 
Lac  de  Flambeau.  (Norwood.) 

Garnet.  —  Lac  de  Flambeau  river,  four  miles  above  the  mouth,  and  other  places  in 
Archaean  rocks.  (Norwood.) 

Epidote. — Associated  with  copper  ores  in  Ashland  and  Douglas  counties. 

Phlogopite  (Rhombic  Mica). — On  the  Eau  Claire  river,  four  miles  above  the  falls,  in 
large  plates.  (Dr.  Littel.) 

Wemerite  (Scapolite).  —  Twin  Falls,  of  the  Menomonee  River  of  Green  Bay.  (Fester 
&  Whitney.) 

Labradorite.  —  An  ingredient  of  trap-rocks;  upper  rapids  of  the  Bois  Brule  river  of  Lake 
Superior.  (Owen.) 

Albite  (White  Feldspar).  —  Common  in  boulders  of  Archsean  rocks. 

Orthodase  (Potash  Feldspar).  —  Common  in  Archaean  rocks.  By  decomposition  forms 
Kaolin  (Potter's  Clay). 


ANNUAL  REPORT  FOR  1873.  29 

Tourmaline.  —  Outlet  of  Lac  de  Flambeau.     (Schookraft.) 
Cyanite  (Kyanite).  —  Lac  de  Flambeau.    (Dr.  Norwood.) 
Laumonite.  —  Copper  veins  on  the  Montreal  river.     (J.  P.  Hodges.) 
Chrysocolla,  (Silicious  Oxide  of  Copper).  —  Wisconsin,  with  carbonate  of  copper.  (Dana,.) 
Prehnite.  —  Accompanying  copper  ores,  Lake  Superior. 
Talc.  —  Ableman,  Sauk  county,  in  quartzite. 

Glauconite  (?)  (Green  Sand).  —  Forming'  layers  in  the  Potsdam  and  Upper  sandstone 
Madison,  Janesville  and  numerous  other  places. 

Sapromte  (Thalite,  Owen).  —  Black  river  (of  Lake  Superior).  Tlrree  miles  above  Kettle 
river. 

Kaolinite.  —  Grand  Rapids,  Wood  county.  Potter's  clay  at  Menasha  and  elsewhere. 
Brick  clay  at  Milwaukee,  Watertown,  Port  Washington,  Sheboygan,  etc.,  making 
brick  of  a  light  cream,  color.  Pipestone  (Catlinite)  in  Barren  county  on  lands  bo- 
longing  to  the  Cornell  University.  There  are  also  clays  so  largely  consisting  of 
silex  in  minute  grains  as  to  be  useful  as  polishing  powders, 

Apatite  (Phosphate  of  Lime).  —  In  the  Potsdam  sandstone  and  in  Galena  limestone  the 
fossil  Lingulae  are  composed  of  phosphate  of  linie. 

Barite  (Sulphate  of  Barites.  Heavy  Spar).  —  Abundant  in  the  lead  region;  Mineral 
Point,  Shullsburg,  etc. 

Cekstite  (Sulphate  of  Strontia). —  In  drift  clay  filling  a  crevice  in  limestone,  Wauwatosa 
near  Milwaukee. 

Anglesite  (Sulphate  of  Lead).  —  In  small  crystal?,  lining  cavities  in  galenite  at  Mineral 
Point. 

Leadhittite.  —  At  Mineral  Point.     (Owen.) 

Gypsum.  — At  Sturgeon  Bay.    Also  among  the  lead  mines. 

Melanterite  (Sulphate  of  Iron,  Copperas).  —  In  the  lead  mines,  formed  by  the  decompo- 
sition of  marcasite  (iron  pyrites). 

Caltite  (Calcareous  Spar,  Tiff).  —  Common  in  the  lead  region.  Fine  crystals  (scalene 
dodecahedrons)  at  Shullsburg.  Coarse  stalactites  in  Cleveland's  Cave,  Dane  coun- 
ty. Tufa  deposited  from  springs  incrusting  moss,  leaves,  sticks,  etc.,  at  numerous 
places.  Travertine  (called  marble)  in  Sauk  and  Richland  counties.  Hydraulic 
limestone  has  been  found  in  some  localities. 

Dolomite.  —  Most  of  the  limestones  of  Wisconsin  contain  magnesia,  and  are  properly 
dolomites. 

Siderite  (Carbonate  of  Iron).  —  Penokee  Iron  Range,  Ashland  county;  rare. 

Smithsonite  (Carbonate  of  Zinc,  Dry  Bone).  —  At  Mineral  Point,  and  other  places  in  the 
lead  region.  Extensively  mined  for  the  manufacture  of  zinc. 

Cerussite  (Carbonate  of  Lead,  White  Lead  ore). — At  Mineral  Point,  Blue  Mounds  and 
elsewhere  in  the  lead  region. 

Hydrozincite  (Calamine,  Zinc  bloom).  — At  Linden  in  a  concretionary  fibrous  crust  on 
Smithsonite  (Whitney). 

Malachite  (Green  Carbonate  of  Copper).  —  In  minute  quantities  in  connection  with 
other  copper  ores,  Mineral  Point,  etc. 

Azitrite  (Blue  Carbonate  of  Copper). — At  Mineral  Point;  Left  Hand  river,  in  minute 
quantities. 

IV.  HYDROCARBON  COMPOUNDS. 

Pztroleum.  —  Some  layers  of  rock  in  the  lead  region  are  highly  bituminous,  burning 
with  a  flame  when  heated. 

Asphaltum.  —  Some  small  cavities  in  the  Devonian  limestone  near  Milwaukee,  and 
also  east  of  Fond  du  Lac,  contain  mineral  tar. 

Peat  is  found  underlying  very  many  of  the  bogs  and  swamps;  sufficient  to  be  of  econo- 
mic value  whenever  the  forests  are  destroyed  and  coal  becomes  scarce. 


30  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

The  following  species  have  been  found  in  the  mining  region  of 
Lake  Superior,  in  Michigan,  and  may  therefore  be  found  in  similar 
localities  in  Wisconsin: 

DonieyMte  (Arsenical  Copper).  Datolite. 

Algodonite  (Arsenical  Copper).  Pectolite. 

Whitneyite  (Arsenical  Copper).  Chlorastrolite. 

Argentite  (Sulphuret  of  Silver).  Apophyllite. 

.Bornite  (Purple  Copper  ore).  Natrolite. 

Covellite  (Indigo  Copper).  Analcite. 

Cerargyrite  (Horn  Silver).  Chabazite. 

Fluorite  (Fluor  Spar).  Harmotome. 

Melaconite  (Black  Oxide  of  Copper).  Stilbite. 

Gothite  (Oxide  of  Iron  and  water).  Heulandite. 

Manganite  (Gray  Oxide  of  Manganese).  Serpentine. 

Wollastonite  (Tabular  Spar).  Gentbite. 

Pyroxene.  Dclessite. 
Pseudomalachite. 

MINERAL  WATERS.  —  Mineral  waters  being  included  among  the 
numerous  objects  to  be  investigated  by  the  survey,  a  beginning  has 
been  made  in  the  collection  of  facts  and  information  in  regard  to 
them,  and  arrangements  made  by  which  it  is  hoped  that  all  desirable 
information  will  be  at  hand,  ready  for  the  final  report. 

Mr.  Gustavus  Bode,  of  the  firm  of  J.  H.  Tesch  &  Co.,  Milwaukee, 
having  already  analyzed  a  number  of  these  waters,  arrangements  were 
made  with  him  to  furnish  corrected  copies  of  his  work  for  the  use  of 
the  survey,  and  to  make  such  further  analyses  as  should  be  deemed 
advisable. 

The  accompanying  table  will  show  in  the  most  compact  and  conve- 
nient form  the  chemical  composition  of  twenty-three  of  the  waters  of 
our  springs,  wells,  rivers,  and  lakes: 


ANNUAL  REPORT  FOR  1873. 


ANALYSES  OF  THE  WATERS  OF  WISCONSIN, 


SUBSTANCES 

IN 

1,000  PARTS. 

Richmond's  Spring, 
Whitewater. 

Market  Square,  Mil- 
waukee. 

fee 
a 

£$ 

11 

W 

Well  at  Waterloo. 

W.  Rahn's  Artesian 
Well,  Manitowoc. 

CM 

£ 

g 

•g 

ft  • 

02  £ 
gr* 

3*  5 

c3  f- 

0 

raj 

be 
i,  . 

|f 

O  te 

a 

Schweickhardt's  Spr. 
Wauwatosa. 

"k 
5) 

ft 

02     . 

,50    g 

P  >•> 

Spring  at  East  Troy. 

Mineral  Rock  Spring, 
Waukesha. 

Nemahbin  Mineral 
Spring,  Delafield. 

Lime  
Magnesia  .  .  . 
Soda  
Potash  
Lithia  



0.274 
0.172 
0.209 
0.014 

0.229 
0.086 
1.508 

0.319 
0.201 
0.399 
0.066 
0.006 

0.844 
0.275 
0.278 
0-007 



0.126 
0.064 
0.043 

0.115 
0.073 
0.011 

0.127 
0.049 
0.032 

0.119 
0.066 
0.011 

0.099 
0.067 
0.022 

0.117 
0.045 
0.029 

S.  Ox.  of  Iron 

0.005 

0.001 
0.002 
0.018 
0.011 

0.187 

Silica  
Sulphur.  Acid 
Nitric  Acid.  . 



0.041 
0.113 

0.123 
0.146 

0.024 
0.138 
0.409 

0.020 
1.492 



0.010 
0.022 

0.035 
0.006 

0.020 
0.012 

0.024 
0.011 

0.019 
0.010 

Chlorine  .  '.  .  . 
Carbon.  Acid 
Org.  matter  . 

Combined  as 
follows  : 
Chi.  sodium  . 
potassium  . 



0.274 
0.370 

2.034 
0.328 

0.657 
0.253 

0.196 
0.190 



0.010 
0.176 

0.003 
0.177 
trace 

0.004 

0.014 
0.163 

0.004 
0.166 

0.003 
0.160 
trace 

0.005 

0.012 
0.151 

0.015 

0.432 
0.026 

3.353 

0.417 

olois 

0.003 

0.016 

0.023 

0.007 

0.019 

0.022 

calcium  .  .  . 
Sulph.  Soda. 

0.032 
0.004 
0-014 

oloso 

6!260 

0.514 

0.384 
0.638 

6!6ii 

6!  050 

61616 

6'.02i 

6'.6i9 

oioi? 

6!6i9 

kme   

magnesia  . 
Nitrate  soda. 
Bicarb,  soda, 
time  
magnesia  . 
iron  
Silica  

0.164 



6!205 
0.643 

0.991 
0.824 















0.038 
0.452 
0.328 
0.012 
0.022 
trace 
0.043 

0.044 
0.369 
0.361 

oloii 

0.130 
0.409 
0.180 

6!i23 

0.188 

61240 
0.281 

9!  024 

6!432 

6!  626 

0.006 
0.249 
0.218 
0.010 
0.013 
0.003 
0.004 

0.016 
0.225 
0.135 

6!6i6 

0.452 

0.009 
0.205 
0.154 
0.007 
0.035 

0.023 
0.227 
0.103 

6'  020 

6!2i2 

0.138 
6!  024 

0.022 
0.176 
0.140 

6  '.019 
trace 

0.021 
0.209 
0.095 
0.001 
0.018 
0.002 

Alumina  .... 
Org.  matter  . 

Total  

0.960 

1.467 

4.643 

2.472 

3.302 

0.507 

0.424 

0.417 

0.400 

0.379 

0.384 

GEOLOGICAL  SURVEY  OF  WISCONSIN. 


ANALYSES  OF  T»E  WATERS  OF  WISCONSIN  —  continued. 


SUBSTANCES, 

IN  1000  PARTS. 

i 

$ 
to 
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cc 

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£ 

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f* 

ci 

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~£  « 
^ 

a 

£ 

fcc 

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A 

cc 

a  cs 
o  "aS 

-—    O 

=£•* 
1-3 

Dousuian's  Trout  Spr'gs, 
Waterville. 

,M 

JSJ 

£ 

fcO 

_S 

a. 
^    . 
v 

*x  3 

~§e 
15 
a 

2 
o 

1 

tn" 

O 

> 

2 

§s 

11 
1" 

1 

Id 

1^ 

•<£ 
o 

£l3 

Sro 

^ 

Harriman's  Min.  Spring, 
Appleton. 

S 

~ci 

1 

'O    QJ 

S  s 

f==i  ^ 
0     5 

-i^ 

»3 

* 

1-g 
oa 

cc 

^"sT 

•i.     rt 

Fft 

a 

cc 
c  o 

II 

< 

Lime  

0.096 

0.108 

0.082 

0.099 

0  101 

0.079 

0  067 

0  Ofi^ 

0  0°>4 

0  048 

0  O/tl 

Magnesia  

0.059 
0.024 

0.060 
0.012 

0.059 
0.037 

0.050 

0.028 

0.039 
0.025 

0.050 
0.015 

0.049 
0.005 

0.040 
0.061 

0.027 
0  043 

0.017 
0  002 

0.018 
0  005 

Potash    

Sesqui  Ox.  of  Iron. 
Alumina  
Silica  
Sulphuric  Acid.  .  .  . 

o.'oii 

0.009 

0.002 
0.002 
0.017 
0.023 

0.006 

6'  026 
0.016 

0.002 
0.002 
0.014 
0.009 

o.'oie 

0.009 

0.004 
0.002 
0.016 
0.010 

6.'  055 
0.009 

o.'ois 

0.049 

0.002 

6'6i5 

0.013 

o.'oie 

0.005 

0.005 

6.'6i:j 

0.028 

Chlorine.  . 

0.008 

0.002 

0.007 

0.007 

0  Oil 

0.00'^ 

0.002 

0  045 

0  004 

0  003 

0  007 

Carbonic  Acid  .... 

0.149 

0:147 

0.147 

0.133 

0.129 

0.139 

0.103 

0.090 

0.095 
0.011 

0.053 

0.037 

Combined  as  fol- 
lows: 
Chloride  of  Sodium. 

0.013 

0.004 

0.012 

0.012 

0.018 

0.004 

0.004 

0.074 

0.006 

0.006 

0.009 

0.005 

Sulphate  of  Soda.  . 

0.015 

0.024 

0-027 

0.016 

0.017 

0.019 

0.007 

0.073 

0.023 

lime  



0.013 



..... 



0.009 

0.010 



0.009 

6'  042 

Bicarbon'e  of  Soda, 
lime  

0.020 
0.171 

6'is3 

0.035 
0.145' 

0.023 
0.170 

0.018 
0  179 

0.008 
0.151 

0.112 

0  105 

0.052 
0.076 

0.079 

6'  072 

magnesia.  ... 

0.125 

0.126 

0  124 

0.106 

0  081 

0  111 

0  103 

0  083 

0  056 

0  035 

0  008 

iron  
Silica  . 

oioii 

0.004 
0.017 

0.010 
0.026 

0.002 
0.014 

6.016 

0.006 
0.015 

o!655 

0.012 

0.003 
0.015 

o.oie 

0.006 
0  013 

Alumina  

0.002 

0.002 

0.002 

trace 

0  Oil 

Total  

0.358 

0.373 

0.379 

0.345 

0.309 

0.316 

0.290 

0.357 

0  242 

0  145 

0  155 

Though  we  have  none  that  can  properly  be  classed  as  "salt  water," 
nearly  every  one  contains  a  small  quantity  of  chloride  of  sodium 
(common  salt),  varying  from  a  mere  trace  up  to  0.423;  the  mean 
(omitting  No.  3  as  exceptional)  being  0.052.  It  is  believed  that  no 
salt  bearing  strata  exist  among  the  rocks  of  Wisconsin,  and  conse- 
quently that  the  production  of  salt  can  never  become  one  of  the  re- 
sources of  our  people. 

A  few  only  of  these  waters  contain  potash  in  small  quantities,  in 

*  A  more  complete  analysis  of  the  water  of  the  Bethesda  spring  will  be  found  in  the  report  ca 
Eastern  Wisconsin,  and  of  the  Sparta  well  in  the  report  of  Mr.  Strong  in  a  subsequent  volume. 


ANNUAL  REPORT  FOR  1873.  33 

combination  with  chlorine.  Epsom  salt  (sulphate  of  magnesia)  is 
found  only  in  two;  sulphate  of  lime  is  equally  rare, being  only  found 
in  two  cases.  The  very  small  amount  of  alumina  is  remarkable, 
where  there  is  so  much  clay  in  the  soil.  The  occurrence  of  chloride 
of  lithium  *  and  nitrate  of  soda  is  also  an  interesting  variation  in  the 
composition  of  these  waters,  being  only  found  in  the  well  at  Water- 
loo. Possibly  the  proximity  of  this  locality  to  the  quiirtzite  (and 
perhaps  other  Archaean  rocks)  may  have  something  to  do  with  this 
variation. 

The  absence  of  nitrogen,  ammonia,  the  bromides,  iodides,  etc.,  will 
be  remarked  by  persons  familiar  with  the  composition  of  mineral 
waters. 

In  seeking  for  the  cause  of  this  unusual  absence  of  mineral  matter 
in  our  spring  waters,  we  must  remember  that  the  geological  history 
of  Wisconsin  differs  essentially  from  that  of  other  countries.  A  large 
proportion  of  the  state  is  underlaid  by  rocks  of  Archaean  age,  an  age 
the  furtherest  remote  from  the  present,  while  the  remainder  is  almost 
exclusively  occupied  by  Silurian  rocks,  they  being  the  oldest  of  the 
fossil  bearing  series.  It  thus  appears  that  during  all  the  ages  of  the 
Carboniferous,  Permian,  Jurassic,  Triassic,  Cretaceous  and  Tertiary 
periods,  Wisconsin  continued  to  be  dry  land,  subject  to  the  abrading, 
and  purifying  action  of  rains  and  frost.  This  is  still  further  attested 
by  the  wonderful  amount  of  denudation  our  strata  have  sustained,  and 
which  it  is  made  the  duty  of  the  survey  to  investigate.  While  the 
Alleghany  and  Rocky  mountains  were  being  uplifted  from  the  depths 
of  the  sea,  Wisconsin  stood  firm,  always  above  its  waters,  always  con- 
tributing of  her  substance  for  the  accumulation  of  the  sedimentary 
rocks  of  the  adjoining  states  —  contributions  which  she  still  continues 
to  make. 

During  all  these  vast  periods,  each  occupying  an  incalculable  length 
of  time,  rains  have  continued  to  fall,  the  waters  have  continued  to 
percolate  through  the  soil  and  porous  rocks,  dissolving  and  carrying 
away  all  soluble  substances.  It  is  not  therefore  wonderful  that  by 
this  time  the  waters  of  the  state  have  an  unusual  degree  of  purity. 
Waters  percolating  through  our  limestones  and  sandstones  can  now 
absorb  but  small  amounts  of  earthy  or  alkaline  salts. 

The  waters  now  examined  are  chiefly  from  the  southern  and  south- 
eastern portions  of  the  state,  where  the  several  magnesian  limestones 
prevail;  and  hence  they  contain,  as  before  stated,  as  chief  ingredients, 
the  carbonates  of  lime  and  magnesia,  resulting  directly  from  the  de- 

*  By  a  typographical  error,  the  quantity  of  lithium  in  the  Waterloo  water  has  been 
overstated;  it  is  correctly  given  in  the  table  above. 
Wis.  SUB.— 3 


34:  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

composition  (aided  by  free  carbonic  acid)  of  these  magnesian  lime- 
stones. "Whether  the  Archaean  rocks  further  north  will  afford  waters 
of  a  different  class,  as  seems  probable,  remains  to  be  determined  in  the 
further  progress  of  the  survey. 

"Waters  percolating  through  the  drift  that  so  completely  covers  and 
conceals  the  rocks,  are  also  found  to  contain  chiefly  lime  and  magnesia 
with  smaller  quantities  of  soda,  chlorine,  iron,  etc.  These  elements 
are  most  usually  combined  with  carbonic  acid,  and  are  the  product  of 
the  solution  of  magnesian  limestone  almost  everywhere  existing  in 
the  form  of  boulders,  gravel,  or  calcareous  sand.  If  we  take  a  lime- 
stone pebble  from  one  of  these  springs,  it  will  usually  be  found  soft 
and  much  decayed  upon  the  surface  by  the  action  of  the  waters,  and 
it  would  be  wonderful  indeed  if  such  waters  should  not  contain  lime, 
or  if  such  rocks  should  not,  in  the  course  of  ages,  be  dissolved  and 
carried  away.  As  the  carbonate  of  magnesia  is  always  associated  with 
the  carbonate  of  lime  in  the  rocks,  so  it  is  in  the  mineral  waters.  In 
general,  the  waters  are  found  to  partake  of  the  character  of  the  rocks 
and  soils  through  or  over  which  they  percolate  or  run. 

The  figures  in  this  table  show  the  number  of  parts  in  one  thousand 
parts  (by  weight)  of  the  water,  which  consist  of  solid  matter  that  re- 
mains  when  the  water  is  evaporated.  If  we  do  not  care  to  consider 
minute  differences  arising  from  changes  of  temperature,  and  the  spe- 
cific gravity  of  the  water,  we  have  only  to  multiply  the  figures  in  this 
table  by  seven,  to  find  the  number  of  grains  in  one  pint;  this  product 
being  multiplied  by  eight  will  show  the  number  of  grains  in  a  gallon. 
The  table  shows,  without  any  change  of  the  figures,  the  number  of 
ounces  in  a  cubic  foot  of  the  water. 

This  decimal  system  of  stating  the  results  of  chemical  analyses  is 
adopted  in  all  cases  except  in  regard  to  mineral  waters,  where  we  of- 
ten find  only  the  number  of  grains  in  a  pint,  a  quart,  or  a  gallon. 
Americans  were  the  first  to  adopt  in  currency  and  coinage  this  simple, 
convenient,  easily  comprehended  and  labor-saving  system,  and  we 
should  not  be  the  last  to  apply  it  in  other  cases.  Its  benefits  are  in- 
ternational. If  we  give  the  number  of  grains  of  solid  matter  in  a 
gallon  of  water,  we  use  a  language  understood,  perhaps,  at  home,  but 
not  anywhere  else;  but  if  we  say  there  are  so  many  parts  in  every 
thousand  parts  of  water,  we  state  a  fact  in  a  manner  that  is  under- 
stood in  every  part  of  the  world.  There  will  be  ten  grains  in  every 
thousand  grains;  ten  pounds  in  every  thousand  pounds;  ten  grains 
in  every  thousand  grams;  and  the  Frenchman,  or  the  men  of 
any  other  nation,  will  not  have  to  search  the  encyclopedia  to  find  the 
value  of  a  grain  or  the  size  of  a  gallon  in  "Wisconsin.  I^o  matter 


ANNUAL  REPORT  FOR  1873.  35 

what  the  system  of  weights  and  measures  may  be  in  any  other  conn- 
try,  the  decimal  system  is  the  same  in  all.  The  general  tendency  of 
our  times  is  towards  simplicity  and  international  uniformity,  espec- 
ially in  coinage,  weights  and  measures,  and  hence  the  adoption  of  the 
decimal  system  should  be  encouraged  in  all  proper  ways. 

Many  of  these  waters,  as  well  as  many  others  not  included  in  the 
table,  are  now  known  from  the  best  of  all  tests,  actual  experience,  to 
possess  valuable  remedial  qualities,  and  they  are  annually  resorted  to 
by  great  numbers  of  invalids,  who,  with  judicious  treatment,  are  al- 
most always  benefited. 

These  analyses  were  all  made  by  Mr.  Bode,  except  No.  1,  Kich- 
mond's,  at  Whitewater,  made  in  1873,  by  Dr.  J.  E.  Garner,  of  Mil- 
waukee, and  No.  6,  the  Oakton  Spring,  at  Pewaukee,  made  in  1872, 
by  Dr.  J.  Y.  Z.  Blaney,  of  Chicago. 

Comparing  these  results  with  the  analyses  of  other  mineral  waters, 
we  are  at  once  impressed  with  the  small  amount  of  mineral  matter 
our  waters  are  found  to  contain,  only  four  having  more  than  one  part 
in  one  thousand;  the  average  of  twenty-two  (No.  3  being  omitted  as 
exceptional)  showing  a  mean  of  0.657,  or  about  two-thirds  of  one  part 
only,  in  one  thousand. 

The  slightest  inspection  of  the  table  will  show  that  the  carbonates 
of  lime  and  magnesia  constitute  the  most  prominent  and  important 
ingredients  of  these  waters.  These,  with  the  carbonate  of  soda,  pres- 
ent in  many  of  them,  bring  the  mineral  waters  of  the  state  into  the 
class  of  alkaline  waters,  and  they  are  arranged  in  the  table  in  accord- 
ance with  the  relative  quantity  of  these  salts,  those  having  the  most 
being  placed  before  those  having  less.  The  average  in  the  whole 
number  (twenty- three)  is  0.365,  or  a  little  more  than  one-third  of  one 
part  in  a  thousand,  and  more  than  half  of  the  total  average  total  quan- 
tity of  solid  matter  in  these  waters. 

The  purgative  salts  (sulphates  of  soda  and  magnesia)  are  found 
only  in  very  small  quantities,  except  in  one  case;  the  mean  of  nine- 
teen waters  (No.  5  omitted)  being  only  0.023. 

Of  the  twenty-three  waters,  ten  only,  or  less  than  half,  contain 
iron,  varying  from  0.001  to  0.012,  the  mean  being  0.006.  This  quan- 
tity, though  apparently  so  small,  seems  to  have  very  useful  medicinal 
effects,  and  it  suffices  to  discolor  objects  over  which  the  waters  run. 
Iron  rust  is  deposited  so  freely  from  the  waters  of  the  several  artesian 
wells  at  Sparta,  that  they  are  not  used  for  cooking  or  for  washing' 
purposes. 

RAIN-FALL.  —  It  is  solely  to  the  clouds  that  we  are  indebted  for  the 
supply  of  water,  in  the  form  of  rain,  hail  and  snow,  to  all  our  lakes, 


36 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


rivers,  springs  and  wells.  The  underground  rivers  reaching  from  tho 
Rocky  mountains,  or  the  highlands  of  Dakota,  exist  only  in  the  im- 
agination. Heavy  or  continuous  rains  cause  the  water  to  rise  in  the 
non-flowing  artesian  wells,  in  the  same  manner  and  for  the  same  rea- 
son that  the  water  in  lakes,  rivers  and  ordinary  wells  rise  under  the 
same  circumstances.  In  dry  weather,  or  during  continued  cold 
weather,  when  the  falling  water  ceases  to  penetrate  the  soil,  the  re- 
verse takes  place,  the  waters  of  lakes,  rivers  and  non-flowing  artesian 
wells  fall  below  their  average  height.  Springs  are  subject  to  the 
same  variation  to  a  considerable  degree;  it  is  only  those  that  have 
their  sources  at  considerable  distances  that  show  but  little  or  no  vari- 
ation during  the  changing  seasons. 

The  mean  monthly  and  annual  amount  of  rain- fall,  at  any  given 
locality  is,  therefore,  an  item  of  great  importance  that  will  often  be 
needed  in  the  prosecution  of  the  survey,  and  hence  I  contribute  the 
following  table,  the  result  of  many  years  of  patient  labor.  It  will 
thus  be  made  accessible  to  engineers,  agriculturists  and  meteorolo- 
gists, who  will  often  have  occasion  to  use  it. 

The  table  shows  the  monthly  and  yearly  amount  of  rain  and  melted 
snow  at  Milwaukee,  latitude  43°  3'  N.,  longitude  87°  56'  W.  The 
observations  for  the  years  1843-48  were  made  by  E.  S.  Marsh,  M.  D. ; 
for  1855-59  and  for  1872-73,  by  Mr.  Charles  Winkler;  for  all  thl 
other  years  by  I.  A.  Lapham. 


TABLE  OF  RAIN-FALL  AT  MILWAUKEE. 


MONTHS. 

1841. 

1843. 

1  844. 

1845. 

1846. 

1847. 

1848. 

1849. 

1850. 

January  .  .  . 
February.  .  . 
March  
April  
May  
June  
July  

0.80 
0.33 

2.26 
1.47 
1.78 
6.13 
3.72 

'  '6.'86' 

1.67 
0.35 

1.66 
3.15 
4.20 
5.34 

5.05 

1.30 
1.73 
1.35 
1.15 

0.78 
3.22 
3.81 

1.92 
0.80 
1.24 
5.33 

1.33 

4.05 
3.18 

1.06 
1.25 
1.40 
2.12 
3.53 
1.75 
1.43 

0.91 

1.12 
1.94 
1.20 
3.60 
4.33 
2.70 

1.20 
0.37 

2.31 
3.24 
4.08 
3.73 
2  36 

0.75 
0.38 
2.85 
2.21 
0.28 
1.98 
1  99 

August  
September  . 
October  
November  . 
December  .  . 

3.85 
7.02 

1.23 

1.70 
4.03 

3.37 
1.57 
1.29 

2.79 
0.85 

3.85 
0.99 
1.74 
1,46 
3.04 

0.80 
4.92 
0.93 
0.24 

0.31 

0.90 
3.27 
0.30 

1.68 
1.26 

1.42 
2.35 
0.83 
4.37 

0.94 

5.10 

2.73 

3.50 
2.50 
3.89 

3.54 
1.25 
3.07 
5.00 
0.94 

9.03 
1.73 

1.00 
2.  SO 
1.43 

Winter.  .  .  . 

2.87 

6.07 

3.03 

3.57 

2  97 

5  46 

2  02 

Spring  
Summer  .  .  . 
Autumn.  .  . 

5.51 
13.70 
9.95 

"s.'es" 

9.01 
14.24 

4.19 

3.28 

7.83 
6.09 

7.90 
8.13 
5.25 

7.05 
4.60 

7.55 

6.74 
12.13 

8.73 

9.63 
9.63 
9.32 

5.37 
13.00 
5.53 

Year  

34.32 

32.50 

20.54 

25.26 

22.45 

33.52 

31.09 

26.41 

ANNUAL  REPORT  FOR  1873. 
TABLE  OF  RAIN-FALL  AT  MILWAUKEE  —  continued. 


37 


MONTHS. 

1851. 

1852. 

1854. 

1855. 

1856. 

1857. 

1858. 

1859. 

1860. 

January  .  .  . 

0.89 

1.13 

4.05 

2.00 

0.10 

2.15 

1.10 

0.53 

February  .  . 

2.51 

1.00 

1.20 

1.00 

1.85 

1.46 

1.20 

1.40 

March  

0.37 

4.56 

1.33 

1.86 

0.15 

1.20 

2.11 

4.42 

033 

April  

1.47 

2.64 

2.07 

1.80 

3.10 

3.69 

5.15 

4.57 

0.33 

May  

6.85 

1.95 

3.73 

1.45 

3.04 

4.60 

8.51 

3.62 

1.34 

4.43 

2.46 

5.76 

3.68 

4.13 

3.41 

4.08 

3.97 

4.15 

July.. 

3.37 

3.27 

6.15 

5.56 

2.26 

3.14 

3.86 

2.08 

1.95 

August  — 

September  . 
October  
November.  . 
December.  . 

3.15 

2.92 
1.32 
2.08 
1.04 

0.58 

2.30 
4.87 
2.72 
1.85 

0.97 
2.81 
3.60 
0.43 

2.03 

3.09 
6.88 
2.01 

1.85 
2.61 

0.91 
2.70 
2.48 
4.42 

2.83 

3.01 
2.73 
3.96 
1.50 
1.70 

2.15 
3.92 
4.59 
4.95 
1.93 

0.27 

2.35 
1-52 
3.12 
0.64 

2.80 
2.50 
2.09 
2.61 
1.99 

\V^nter    . 

4  83 

3.17 

7.28 

5  61 

4  78 

5  31 

4  23 

2  57 

Sprin0"  

8.69 

9.15 

7.13 

5.11 

6.29 

9.49 

15.77 

12.61 

4.00 

Summer  .  .  . 
Autumn  .  .  . 

10.95 
6.32 

6.31 

9.89 

12.88 
6.84 

12.33 

10.74 

7.30 
9.60 

9.56 
8.19 

10.09 
13.46 

6.32 
6.99 

8.90 
7.20 

Year  

30.40 

29.33 

36.04 

29  02 

30.89 

44.86 

28  86 

24  02 

MONTHS. 

1861. 

1862. 

1863. 

1864. 

1865. 

1866, 

1867. 

1868. 

1869. 

January  
February  .  .  . 
March  

2.15 
3.34 
1.53 

3.41 
0.48 

2.10 

3.33 

1.85 
2.48 

2.15 
0.42 
2.52 

0.22 

3.58 
3.89 

2.58 
1.64 
1.50 

2.61 
2.13 
1.81 

1.29 

0.92 
4.59 

2,51 
2.76 
1.17 

April  ...... 

3.65 

5.34 

1.04 

3.01 

1.96 

8.04 

1.73 

2.97 

3.90 

TVTav.  . 

4.32 

5.11 

5.21 

2.74 

1.11 

2.06 

4.39 

2.05 

4.77 

1.80 

3.86 

0.79 

0.15 

3.57 

4.83 

2.04 

5.78 

7.67 

July.. 

4.87 

4.09 

2.41 

7.07 

1.78 

2.73 

2.60 

3.73 

2.76 

Aug-ust  
September.  . 
October  .... 
November.  . 
December.  . 

2.21 
3.39 
1.48 
1.59 
1.55 

2.94 
5.03 
8.26 
1.28 
1.37 

2.62 
1.02 
2.97 
3.15 
4.57 

0.61 
2.93 
1.63 
2.61 
1.99 

4.34 
4.67 
4.13 
0.31 

0.52 

3.95 
4.55 
2.76 
1.32 
3.00 

2.01 
1.46 
0.80 

1.53 

1.51 

1.85 
0.90 

1.18 
3.23 

0.88 

3.70 
1.97 
0.46 

3.35 

2.79 

Winter  
Spring  
Summer.  .  .  . 
Autumn.  .  .  . 

7  48 
9.50 
8.88 
6.46 

5.44 
12.55 

10.89 
9.57 

6.55 

8.73 
5.82 
7.50 

7.14 

8.27 
7.83 
7.17 

5.79 
6.96 
9.69 
9.11 

4.74 
6.60 
11.51 
8.63 

7.74 

7.93 
6.65 
3.79 

8.72 
9.61 
11.36 
5.31 

6.15 

9.84 
14.13 

5.78 

Year  

31.88 

38  27 

31.80 

27.83 

30.08 

33.96 

24  62 

29  37 

37  81 

38  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

TABLE  OP  RAIN-FALL  AT  MILWAUKEE  —  continued. 


MONTHS. 

1870. 

1871. 

1872. 

1873. 

No.  of 
Years. 

Mean. 

2.37 

3.14 

0.57 

2.39 

29 

1.73 

1.32 

1.32 

0.36 

1.50 

29 

1.36 

5.01 

2.75 

0.80 

1.48 

30 

2.10 

0.51 

3.30 

2.50 

2.70 

30 

2.68 

0.63 

2.24 

3.10 

4.89 

30 

3.24 

June    

2.62' 

3.03 

4.42 

3.40 

30 

3.69 

July  

4.64 

1.84 

1.93 

1.82 

31 

3.20 

August  •••  

2  69 

3.77 

2.64 

5.26 

31 

2.82 

September  

2.10 

0  60 

8.87 

2.57 

31 

3.07 

1.99 

2.72 

0.82 

2.12 

31 

2.15 

November  

0.94 

2  40 

1.80 

1.40 

31 

2.31 

1.79 

2.03 

1.00 

2.81 

31 

1.91 

"Winter  

6.48 

6.25 

2.96 

4.89 

5.00 

6.15 

8  29 

6.40 

9.07 

8.02 

9.95 

8.64 

8.99 

10.48 

9.71 

5.03 

5.72 

11.49 

6.09 

7.53 

Year  

26.61 

29.14 

28.81 

82.34 

30.27 

This  table  shows  that  the  rain  in  Wisconsin  is  generally  very  well 
distributed  through  the  several  months,  seasons  and  years;  the  gen- 
eral average  for  thirty-one  years  being  30.27  inches,  varying  from. 
20.54:  in  1845,  to  44.86  in  1858;  the  greatest  amount  in  any  one  month 
was  9.03  inches  in  August,  1850,  and  the  least  0.10  in  January,  1857. 
The  most  rain  upon  an  average  falls  in  June;  the  least  in  February; 
the  three  months  of  summer  have  been  supplied,  upon  the  average, 
with  the  most  rain,  the  three  months  of  winter,  the  least;  while  the 
spring  months  have  a  little  more  than  those  of  autumn. 

During  nearly  half  the  years  covered  by  the  table  the  rain -fall  dif- 
fered but  little  from  the  general  mean ;  while  nine  were  considerably 
in  excess,  and  eight  were  supplied  with  less  than  28  inches. 

From  the  published  results  of  observations  collected  by  the  Smith- 
sonian Institution,  it  appears  that  the  average  rain-fall  at  about 
twenty  stations  in  Wisconsin,  or  on  its  immediate  border,  was  about 
three  inches  more  than  at  Milwaukee. 

The  annual  supply  of  falling  water,  as  shown  by  this  table,  is 
equivalent  to  a  sheet  of  water  two  and  three-fourths  feet  deep,  spread 
evenly  and  uniformly  over  the  whole  area  of  the  state.  The  most  care- 
ful investigations  have  shown  that  this  is  sufficient  to  account  for  the 

O 

outflow  of  all  our  lakes,  rivers  and  springs ;  the  total  quantity  thus 
carried  away  being,  in  our  climate,  found  equivalent  to  only  about 
one-fourth  of  the  total  rain-fall.  The  remainder  is  evaporated,  and 
thus  returned  to  the  atmosphere,  either  directly  from  the  surface,  or 
after  having  performed  service  in  the  growth  of  plants.  The  quantity 


ANNUAL  REPORT  FOR  1873.  39 

of  water  absorbed  by  the  roots  of  plants,  with  its  mineral  contents, 
and  then  evaporated  from  the  leaves,  is  enormous. 

Rain  water  soon  penetrates  the  soil  and  finds  its  way  through 
crevices  and  pores  of  the  more  solid  rock  strata,  down  to  very  con- 
siderable depths,  dissolving  such  substances  as  are  soluble  and  carry- 
ing them  to  distant  places.  It  is  here  we  must  look  for  the  origin 
of  all  mineral  waters,  and  for  the  cause  of  a  large  share  of  the  de- 
nudation which  in  the  lapse  of  many  ages  has  become  so  very  con- 
siderable. 

Knowing  this  annual  quantity  of  water-supply  and  outflow,  with 
the  amount  of  mineral  matter  it  carries,  we  lack  only  a  knowledge  of 
the  amount  of  matter  mechanically  suspended  in  running  water,  de- 
rived from  the  loose  soil  and  from  abraded  rocks,  to  be  able  to  cal- 
culate the  time  required  for  the  excavation  of  any  given  valley  whose 
dimensions  are  known. 

The  gradual  decay  and  wearing  away  of  rocks  is  not  confined  to  the 
limestones  and  softer  rocks,  but  includes  many  of  the  older  and  harder 
kinds,  especially  such  as  contain  feldspar  and  similar  minerals.  Rocks 
are  always  penetrated  with  water  and  they  hold  in  their  pores  an 
average  of  five  or  six  per  cent,  by  weight ;  a  hundred  pounds  being 
capable  of  absorbing  five  or  six  pounds  of  water.  As  the  clouds 
afford  a  constant  supply  which  is  continually  removed  in  under- 
ground currents,  springs  and  rivers,  carrying  with  it  the  mineral 
matter  taken  up,  we  have  a  perpetually  recurring  cause  of  geological 
change.  During  the  progress  of  water  through  the  different  rocks, 
meeting  with  different  chemical  elements,  many  chemical  changes 
probably  occur  in  the  substances  taken  up,  and  it  is  only  the  final 
result  of  all  these  changes  that  we  find  in  the  mineral  spring  as  it 
appears  at  the  surface.  Any  considerable  change  of  the  course  of  the 
water  among  the  rocks  would,  therefore,  lead  to  changes  in  the  com- 
position or  combination  of  ingredients  it  contains. 

"Water  when  pure  has  but  little  power  to  dissolve  mineral  matters, 
but  when  combined  with  carbonic  acid,  this  dissolving  power  is  very 
much  increased.  When  waters  holding  these  substances  reach  the 
open  air  they  give  off  the  excess  of  carbonic  acid,  and  hence,  by  losing 
a  portion  of  their  dissolving  power,  become  unable  to  hold  them,  and 
they  are  deposited  forming  a  coating  to  sticks  and  stones  over  which 
they  may  run. 

If  this  deposit  consists  chiefly  of  lime,  and  accumulates  with  con- 
siderable rapidity,  such  springs  are  known  as  petrifying  springs,  or 
lime  springs,  of  which  we  have  many  examples.  The  deposit  often 
forms  considerable  conical  mounds  surrounding  the  spring;  and  moss, 


40  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

leaves,  shells,  sticks,  etc.,  are  often  incrusted  in  such  manner  as  to 
preserve  beautifully  their  peculiar  markings. 

In  many  cases  the  oxide  of  iron  is  thus  thrown  down,  discoloring 
everything  over  which  the  water  runs.  The  quantity  of  iron  thus 
deposited  does  not  depend  so  much  upon  the  absolute  quantity  of 
iron  in  the  composition  of  the  water  as  upon  the  feebleness  with 
which  it  is  held  in  solution.  Such  springs  are  called  chalybeate,  or 
iron  springs. 

Sulphuretted  hydrogen,  which  gives  the  sulphur  taste  and  odor  to 
many  springs,  is  supposed  to  result  from  the  decomposition  of  or- 
ganic (animal  or  vegetable)  matter  —  mostly  of  vegetable  origin.  Such 
springs  are  called  sulphur  springs,  and  we  have  several  examples  in 
the  state. 

The  rock  strata  are  clearly  shown,  by  the  evidence  of  marine  fossil 
shells  and  corals,  to  have  been  originally  deposited  in  the  waters  of 
an  ancient  sea,  from  which  they  have  been  elevated  to  form  our 
present  continent;  and  it  is  not,  therefore,  wonderful  that  they  should 
yield  to  the  percolating  waters  those  elements  which  we  find  in 
mineral  waters.  The  supply  might  be  supposed  to  diminish  as  ages 
pass  by,  but  never  to  become  exhausted. 

All  natural  waters  may  be  regarded  as  "mineral  waters"  —  for 
none  are  absolutely  pure.  Indeed  it  is  probable  that  pure  water,  such 
as  can  only  be  obtained  by  careful  distillation,  would  not  sustain 
either  animal  or  vegetable  life.  Even  rain  water  is  found  to  contain 
minute  quantities  of  salt,  of  ammonia,  soda,  lime,  and  organic  matter, 
with  traces  of  many  other  substances.  It  is  mainly  from  the  mineral 
matters  dissolved  in  water  that  plants  derive  their  solid  materials  con- 
stituting the  ash.  The  silica,  though  small  in  amount  in  water,  is  of 
great  importance  to  the  growth  of  plants,  especially  the  grasses,  in- 
cluding the  cereals,  etc. ;  all  our  waters  contain  silica. 

Springs,  whose  sources  are  near  the  surface,  are  apt  to  contain  mat- 
ters resulting  from  the  decay  of  organic  matter,  and  other  deleterious 
material.  Those  which  come  from  greater  depths,  and  .have  passed 
over  greater  distance,  are  supposed  to  be  of  greatest  value ;  the  organic 
matter  having  been  absorbed  in  passing  through  the  soil  and  rocks. 
Such  springs  usually  assume  a  temperature  showing  little  change 
from  winter  to  summer,  and  which  correspond,  with  the  mean  annual 
temperature  of  the  place. 

Several  of  these  waters,  notably  those  of  Fond  du  Lac,  Sparta,  and 
Watertown,  are  known  as  magnetic;  the  iron  tubes  through  which 
they  flow,  possessing  the  magnetic  property  in  a  high  degree.  Whether 
this  magnetic  quality  has  any  medicinal  value  remains  yet  to  be  de- 


ANNUAL  REPORT  FOR  1873.  41 

termined.  A  French  savan  has  endeavored  to  demonstrate  that  the 
medicinal  value  of  mineral  waters  is  mainly  due  to  their  electrical 
condition;  and  the  subject  is  well  worthy  of  investigation  by  those 
most  interested  in  it;  and  those  who  have  the  opportunity. 

There  are,  in  this  state,  many  other  springs  and  wells,  not  included 
in  the  table  above,  that  have  been  brought  to  the  notice  of  the  public 
for  their  medicinal  virtues;  among  them  the  following,  all  at  Wauke- 
sha:  Hygiene,  Mount  Horeb,  Bars  tows,  White  Eock,  and  Fountain 
Springs. 

Progress  has  been  made  towards  the  compilation  of  a  list  of  all  the 
more  important  springs,  including  those  noted  as  petrifying  (lime), 
chalybeate,  sulphur  springs,  etc.,  and  also  such  as  are  of  sufficient 
capacity  to  supply  ponds  for  the  artificial  rearing  of  fish. 

The  investigation  of  mineral  waters  cannot  be  said  to  be  complete 
without  a  determination  of  the  gaseous  matters  they  contain,  for  these 
may  materially  modify  the  medicinal  or  other  effects  of  the  solid  in- 
gredients. This  can  only  be  done  at  the  spring,  with  water  taken  at 
the  moment  it  reaches  the  open  air. 

RELATION  OF  THE  GEOLOGICAL  SURVEY  TO  AGRICULTURE.  —  The  law 
providing  for  a  geological  survey  of  the  state  of  Wisconsin,  includes 
also,  and  very  properly,  provision  for  some  work  for  the  special  inter- 
est of  agriculture;  it  being  now  generally  known  and  admitted  that 
these  two  subjects  are  so  intimately  related,  that  whatever  is  done  to 
increase  our  knowledge  of  the  local  and  special  geology  of  any  dis- 
trict tends,  at  the  same  time,  to  promote  the  interest  of  the  farmer 
cultivating  land  in  the  same  district.  The  underlying  rocks  are  exam- 
ined as  to  their  chemical  composition,  and  surface  arrangement  or 
geographical  extent;  they  are  the  sources  from  whence  is  derived  the 
very  soil  into  which  the  farmer  annually  intrusts  his  seed.  Their  dip, 
order  of  succession,  depth  beneath  the  surface,  their  porous  or  imper- 
vious nature;  these  are  the  data  for  deciding  about  artesian  or  other 
wells,  often  the  only  resource  for  a  permanent  supply  of  water  for 
farm  purposes;  and  as  the  forests  become  reduced  in  extent,  the 
necessity  for  such  wells  will  be •  gradually  increased.  The  drift  phe- 
nomena, gleaned  from  an  extended  and  careful  study  of  the  loose  ma- 
terials covering  and  concealing  the  more  solid  rocks,  left  here  by  the 
glaciers  of  the  ice  period,  the  study  of  which  is  so  interesting  to  the 
practical  and  speculative  geologist,  have  been  the  means  of  diffus- 
ing and  spreading  the  soil  over  the  rocky  surface,  commingling  and 
mixing  the  various  clays,  sands,  and  pebbles,  derived  from  the  disinte- 
gration of  the  rocks,  in  such  manner  as  to  render  them  the  best  suited 


42  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

for  the  growth  of  vegetation.  The  mineral  and  other  native  resources 
are  discovered  and  made  known ;  they  are  the  material  for  various  man- 
ufactures, and  their  development  creates  a  home  market  —  the  best  of 
all  markets  —  for  farm  products;  thus  deciding  the  great  question, 
now  so  much  agitated,  relating  to  cheap  transportation,  by  avoiding 
the  necessity  of  any  transportation  of  these  products. 

The  barometrical  measurements  of  the  heights  and  depressions, 
required  of  the  survey,  will  shew  in  many  cases  the  sources  of  water 
supply  upon  which  we  are  dependent  for  this  life-giving  element. 
These  are  taken  as  data  in  the  topographical  survey,  which  is  to  show 
the  general  contour  of  the  ground,  the  extent,  elevation,  arid  slope  of 
drainage  basins,  or  river  valleys ;  the  amount  and  value  of  water  power 
afforded  by  these  rivers  j-  the  proportion  of  timbered,  open,  and  prairie 
land;  the  uplands,  the  swamps,  and  marshes;  all  such  detailed  inform- 
ation is  of  importance  to  various  interests,  and  especially  to  the  agri- 
culturist. The  geodetic  survey,  which  has,  through  the  instrumen- 
tality of  the  geological  survey,  been  extended  into  Wisconsin  by  the 
general  government,  will  also  aid  in  the  development  of  the  topo- 
graphical features  of  the  state,  and  will  show  with  greater  accuracy 
the  exact  position  of  the  principal  lines  of  the  government  surveys, 
from  which  are  derived  and  established  the  boundaries  of  farm  lands, 
thus  often  preventing  litigation  and  neighborhood  quarrels. 

It  is  further  made  the  duty  of  the  survey  to  search  for  and  properly 
examine  all  mineral  fertilizers  that  may  exist  in  the  state;  to  analyze 
the  clays,  peats,  marls  and  other  natural  products  useful,  either  in 
maintaining  the  richness  of  the  soil  or  of  restoring  it  when  exhausted 
by  the  injudicious  management  of  ignorant  and  selfish  men.  The 
soils  and  subsoils  are  to  be  made  subjects  of  study,  and  observations 
are  to  be  made  upon  the  animal  and  vegetable  products  with  refer- 
ence to  their  agricultural  interest.  Specimens  are  to  be  collected  ex- 
emplifying the  geology  of  the  state,  which  are  to  be  deposited  with 
the  various  institutions  of  education,  from  which  the  youth  of  our 
state  may  hereafter  acquire  that  more  definite  knowledge  of  our  local 
geology  which  will  enable  them  to  prosecute  their  future  labors  in  farm- 
ing with  greater  advantage  both  to  themselves  and  to  the  country. 

It  is  now  very  generally  admitted  that  the  chemical  analysis  of 
soils  does  not  lead  to  all  of  the  beneficial  results  that  were  formerly 
anticipated  from  this  source.  The  healthy  growth  of  farm  crops  is 
dependent  upon  too  many  varying  conditions,  besides  the  mere  quan- 
tity of  plant-food  that  may  exist  in  the  soil,  to  enable  the  chemist  to 
detect  the  cause  of  any  given  failure,  by  soil  analysis.  It  was  once 
supposed  that  we  had  only  to  analyze  a  soil  before  and  after  a  crop 


ANNUAL  REPORT  FOR  1873.  43 

has  beea  taken  from  it,  to  detect  the  substances  that  had  been  ab- 
stracted, and  thus  indicate  what  should  be  artificially  supplied  to 
stimulate  the  growth  of  the  next  crop;  but  such  is  the  minuteness  of 
the  quantity  of  plant-food  compared  with  the  mass  of  the  soil,  that 
chemical  science  has  not  yet,  except  to  a  limited  extent,  been  able  to 
accomplish  this  task.  Consequently  no  general  effort  will  be  made  to 
analyze  the  soils  of  the  state;  but  if  any  are  found,  that,  from  any 
special  peculiarity  or  other  reason,  seem,  to  require  it,  such  analysis 
will  be  made. 

Geology  is  now  very  properly  included  among  the  studies  to  be 
pursued  in  agricultural  colleges,  with  a  view  to  its  special  advan- 
tages in  the  proper  cultivation  of  the  soil  —  a  cultivation  which  shall, 
without  the  least  diminution  of  its  annual  product,  perpetually  main- 
tain its  fertility.  Every  farmer  should  know  whether  his  land  is  un- 
derlaid by  rocks  whose  disintegration  is  beneficial  or  otherwise; 
whether  these  rocks  are  of  the  granitic  kinds,  or  whether  they  consist 
of  sandstone,  limestone  or  shales.  He  should  also  be  able  to  deter- 
mine the  nature  of  the  pebbles,  small  and  large,  abounding  in  his 
fields,  the  gradual  decay  of  which,  from  year  to  year  by  reason  of  ex- 
posure to  weather  changes  —  frost,  rain,  sunshine  and  alternate  ex- 
posure to  heat  and  cold  —  will  add  useful  or  useless,  or  even  delete- 
rious qualities  to  the  soil.  Limestone  pebbles  especially,  by  their 
gradual  disintegration,  are  of  the  greatest  value  by  restoring  fertil- 
izing substances  to  the  soil  that  would  otherwise  soon  be  exhausted 
by  continual  cropping.  If  these  pebbles  are  of  such  quality  as  to  be 
thus  beneficial,  the  land  possesses  additional  value;  if  otherwise,  a 
larger  annual  expense  for  fertilizers  will  be  required.  The  system  of 
farm  management,  suited  to  the  one  case,  would  require  modification 
for  the  other.  Hence  it  is  sufficiently  apparent  that  some  knowledge 
of  geology  is  quite  essential  to  the  intelligent  farmer,  and  that  it  is 
wise  to  include  it  in  a  course  of  studies  to  be  pursued  in  our  agricul- 
tural colleges. 

The  several  reports  to  be  made  to  the  governor  annually  in  Janu- 
ary, though  chiefly  intended  to  make  known  the  progress  and  results 
of  each  year's  work,  will  be  found  to  contain  much  that  is  of  interest 
to  the  farmer.  The  publication  and  general  distribution  of  reports 
of  geological  surveys  always  prove  beneficial,  by  calling  public  atten- 
tion, in  an  official  and  reliable  manner,  to  the  resources  and  advan- 
tages of  the  district  surveyed,  for  the  agricultural,  manufacturing 
and  other  interests. 


44:  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

LIST  OF  MAPS 
Accompanying  the  First  Annual  Report  of  the  Wisconsin  Geological  Survey,  1873. 

A  map  of  the  state  (published  by  Silas  Chapman)  on  a  scale  of  six  miles  to  an  inch, 
showing  in  colors  the  boundaries  and  extent  of  the  several  rock  formations  so  far  as 
is  known  up  to  the  end  of  the  year  1873.    On  four  sheets. 
A  map  of  the  Muscalonge  diggings  in  Grant  county,  on  a  scale  three  chains  (198  feet) 

to  an  inch. 

A  map  of  Ashland  county  and  another  of  Douglas  county,  on  a  scale  of  two  miles  to  one 
inch,  showing  the  geological  features  and  mineral  ranges  in  those  counties;  also  a 
map  of  the  Apostle  Islands;  to  accompany  the  report  of  Prof.  R.  D.  Irving. 
A  map  in  two  sheets  on  a  scale  of  two  miles  to  an  inch,  showing  the  geology  and  topo- 
graphy of  the  region  surveyed  by  Prof.  T.  C.  Charnberlin,  from  the  state  line  in 
Wai  worth  and  Rock  counties  to  Keshena,  in  Shawano  county.  Also  two  maps,  on 
a  scale  of  six  miles  to  an  inch  (based  upon  Mr.  Chapman's  map);  one  showing  the 
distribution  of  vegetation,  etc.,  the  other  representing  the  areas  occupied  by  the 
different  kinds  of  soil  in  the  same  region.  These  maps  accompany  the  report  of 
Prof.  Chamberlin. 
Geological  Map  of  the  Lead  Region  (in  part)  on  six  sheets,  to  wit: 

1st.  Ranges  two  and  three  east  from  three  miles  south  of  the  state  line  to  Min- 
eral Point,  being  townships  No.  one,  two,  three  and  four,  in  those  ranges. 
2d.    Townships  four  and  five  in  ranges  one  to  six  west,  inclusive. 
3d.   Townships  four  and  five  in  ranges  one  to  five  east,  inclusive. 
4th.  Ranges  two  and  three  east,  in  townships  five  to  nine,  inclusive. 
5th.  Ranges  two  and  three  east,  in  townships  ten,  eleven,  twelve  and  thirteen. 
6th.  Ranges  five  and  six  east,  from  township  five  to  the  Wisconsin  river  in  town- 
ship nine. 

Topographical  Map  of  the  Lead  Region  (in  part)  on  two  sheets,  to  wit : 
1st.  Ranges  two  and  three  east,  in  townships  one  to  six,  inclusive. 
2d.  Townships  four  and  five  in  range  one  east,  and  ranges  one  to  six  west,  inclusive. 
These  maps  are  all  upon  a  scale  of  one  mile  to  an  inch. 

A  geological,  topographical  and  subterranean  map  of  the  Blue  Mounds  and  the  Brig- 
ham  Lead  Mines,  on  a  scale  of  one  to  twenty  thousand. 
All  these  maps  in  the  lead  region  accompany  the  report  of  Mr.  Moses  Strong. 

All  of  which  is  respectfully  submitted. 

I.  A.  LAPHAM, 

Chief  Geologist. 
MILWAUKEE,  January,  1874. 


ss 


EEPORT  OF  PROGRESS  AND  RESULTS, 

FOR  THE  YEAR  1874. 


BY  I.   A.   LAPHAM. 


During  the  past  year  the  same  parties  have,  been  in  the  field  as  in 
the  preceding  year,  and  in  addition  a  party  under  the  charge  of  Maj. 
T.  B.  Brooks,  late  of  the  Michigan  Geological  Survey,  as  will  be  men- 
tioned in  a  subsequent  part  of  this  report.  I  am  glad  to  be  able  to 
state  that  the  survey  is  progressing  with  reasonable  rapidity;  the 
amount  of  work  done  being  considerably  in  excess  of  that  of  1873. 

The  first  annual  report  of  progress  and  results  of  the  survey  was 
deposited  in  the  office  of  the  governor  on  the  first  Monday  in  Janu- 
ary, 1874,  with  ample  maps  and  illustrations,  accompanied  by  the  re- 
ports of  the  several  assistants.  It  was  found  impracticable  to  com- 
plete the  reports  of  explorations  made  by  the  several  parties  in  1873, 
in  as  full  detail  as  is  desirable,  in  time  to  be  presented  to  the  gover- 
nor on  the  day  required  by  law.  They  were  accordingly  presented  in 
an  unfinished  condition,  with  the  expectation  that  additional  matter 
could  be  annexed  when  prepared.  By  a  law,  approved  March  4th, 
1874,  it  was  provided  that  the  manuscript  report  of  the  geological 
survey  then  made,  with  the  maps  and  drawings,  should  be  bound  and 
preserved  in  the  vaults  of  the  office  of  the  secretary  of  state  at  Madi- 
son; hence  all  such  additional  matter  is  necessarily  excluded,  and  is 
herewith  submitted  in  the  form  of  supplementary  reports. 

For  greater  convenience  in  binding  and  in  future  publication,  it 
was  decided  to  make  all  sections,  drawings,  and  maps,  so  far  as  was 
practicable  upon  sheets  of  uniform  size;  and  rules  were  adopted  to 
secure  uniformity  in  respect  to  the  position  of  maps  and  profiles  upon 
the  sheets. 

Tracings  from  the  township  plats  of  the  government  land  survey 
were  furnished  to  the  several  parties  as  needed;  and  as  before,  they 
were  greatly  assisted  by  the  published  maps  of  the  several  counties. 


46  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

These  are  especially  valuable  as  showing  the  location  of  the  public 
roads,  usually  from  actual  survey. 

The  specimens  collected  during  the  year,  for  study  and  comparison, 
with  the  duplicates  intended  for  the  Academy  of  Sciences,  University, 
colleges,  .and  normal  schools,  now  amount  to.  a  very  considerable 
number,  requiring  much  room  and  involving  some  expense  for  their 
storage  and  proper  arrangement  for  convenient  reference  in  making 
up  the  reports. 

Nearly  five  hundred  townships  (about  one-third  of  the  total  area  of 
the  state)  have  now  been  examined,  with  more  or  less  minuteness,  by 
the  several  parties,  as  follows: 

By  Prof.  Irving  in  1873,  45  townships. 

1874,     -  -     08  « 

By  Prof.  Chamberlin  in  1873,  75  " 

1874,    -  -  130  " 

By  Mr.  Strong  in  1873,    -  50  " 

1874,  -    66  " 

By  Maj.  Brooks  in  1874,  17  " 

By  Mr"  Ives  in  1874,  -       7  " 

Several  of  the  aneroid  barometers  purchased  for  the  survey,  having 
been  found  to  be  imperfect  and  useless,  others  of  better  quality,  which 
have  proved  quite  satisfactory,  were  obtained  directly  from  the  makers 
in  London,  England. 

PROF.  R.  D.  IKVING'S  PARTY.  —  Prof.  Irving  was  directed  to  make 
such  explorations  and  surveys  as  would  enable  him  to  construct  a  geo 
logical  map  and  section  along  a  line  extending  from  the  south  part  of 
Dane  county,  northward,  through  portions  of  Columbia,  Adams,  and 
Wood  counties,  to  Grand  Rapids,  and  thence  up  the  Wisconsin  rivei* 
to  Wausau;  the  breadth  occupied  to  embrace  two  or  three  ranges  of 
townships;  thence  along  the  southern  boundary  of  the  Archaean  rocks 
in  Wood,  Clark,  and  Jackson  counties,  he  was  to  extend  his  work 
westward  to  the  Black  River  Falls;  the  details  of  this  important 
locality  having  been  previously  examined  by  him.  This  route  would 
enable  him  to  determine  many  important  questions,  in  a  portion  of 
the  state  heretofore  but  little  known  geologically ;  especially  in  regard 
to  the  quartzites,  conglomerates,  and  other  rocks  of  the  Baraboo 
river;  the  sandy  region  north  of  Portage;  the  kaolin  beds;  the 
Mosinee  hills;  and  the  reported  localities  of  iron  ores.  As  the  iron 
ores  of  Lake  Superior  and  the  Menomonee  region  extend  through 
considerable  distances,  it  was  hoped  that  there  might  be  a  similar 


ANNUAL  REPORT  FOR  1874.  47 

range  of  ore  beds  extending  eastward  from  Black  River  Falls ;  a  very 
important  question  that  might  be  determined,  by  the  explorations 
thus  to  be  made. 

Before  commencing  the  field-work  of  the  season,  Prof.  Irving  pre- 
pared the  supplementary  report  herewith  submitted,  embracing  de- 
tails of  results  attained  in  1873,  which,  for  want  of  time  could  not,  as 
before  stated,  be  included  in  his  general  report  for  that  year,  now  de- 
posited in  the  office  of  the  secretary  of  state.  This  supplementary 
report,  covering  seventy-four  pages  of  manuscript,  with  several  maps, 
diagrams  and  sections,  will  be  found  to  contain  much  additional  mat- 
ter relating  to  the  geology  of  Douglas,  Bayfield  and  Ashland  counties. 

The  rocks  in  this  part  of  the  state  are  referred  to  five  different  per- 
iods, as  follows: 

1st.  Laurentian  —  Granite,  etc. 

2d.    Huronian  —  Iron-bearing  series. 

3d.    Copper-bearing  rocks. 

4th.  Potsdam  sandstone. 

5th.  Quaternary  —  Drift,  etc. 

Many  facts  and  arguments  are  adduced  to  show  that  this  is  the 
proper  order  of  arrangement,  and  ample  details  are  given,  so  that  geo- 
logists may  judge  of  the  correctness  of  these  views. 

Prof.  Irving  has  been  able  to  show  the  existence  of  a  synclinal  axis 
extending  in  a  southwesterly  direction,  through  these  counties,  being 
the  westward  inland  extension  of  the  great  trough  between  Keweenaw 
Point  and  Isle  Royale,  occupied  mostly  by  the  waters  of  Lake  Super- 
ior. We  thus  have  a  more  clear  understanding  of  the  different  direc- 
tions assumed  by  the  dip  of  the  rocks  at  different  localities,  and  are 
brought  to  a  knowledge  of  one  of  those  grand  movements  in  the  re- 
mote past,  by  which  the  solid  rocks  have  been  folded,  contorted,  and 
lifted  to  their  present  complicated  positions.  To  understand  these 
ancient  disturbances  of  the  strata  is  not  only  a  matter  of  interest  in, 
speculative  geology,  but  is  also  one  of  the  greatest  practical  import- 
ance to  the  miner  and  to  all  having  occasion  to  deal  with  these  rocks. 

It  will  be  seen  that  the  Copper-bearing  rocks  are  Pre-Silurian, 
though  not  as  old  as  the  Huronian.  Prof.  Irving's  conclusions  on 
this  point  are  that: 

1st.  "  The  beds  of  the  Copper-bearing  series  and  those  of  the  Huro- 
nian were  once  spread  horizontally  over  one  another,  including  the 
whole  series  of  tilted  sandstone  on  the  Montreal  river;  they  were  dis- 
turbed by  the  same  force,  and  received  their  present  tilted  positions  at 
the  same  time,  as  evinced  by  the  entire  conf  ormability  of  the  two  series. 


48  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

2d.  "  The  horizontal  sandstones  of  the  Apostle  Islands,  and  the  west 
end  of  Lake  Superior,  were  laid  down  subsequent  to  this  tilting,  and 
also  to  an  immense  amount  of  erosion ;  and  the  sandstones  of  eastern 
Lake  Superior  were  formed  at  the  same  time.  These  points  are 
proved  by  (1)  the  occurrence  of  horizontal  sandstones  in  immediate 
proximity  to  tilted  sandstones  and  traps,  in  Ashland  county;  (2)  the 
occurrence  of  the  same  in  the  Apostle  Islands,  within  but  a  few  miles 
of  the  tilted  beds  of  the  Montreal;  (3)  the  actual  contact  of  the  hori- 
zontal sandstones  with  the  melaphyrs  of  the  Copper-bearing  series  in 
Douglas  county;  and  (4)  similar  and  additional  facts  observed  by 
Messrs.  Brooks  and  Pumpelly  in  the  upper  peninsula  of  Michigan. 

3d.  "  That  hence  the  Copper-bearing  rocks  should  rather  be  classed 
with  the  Archaean  than  with  the  Silurian  rocks." 

Under  the  head  of  "Economic  Geology,"  Prof.  Irving  discusses  the 
questions  regarding  the  probable  existence  of  copper,  silver,  etc.,  with 
an  account  of  the  attempts  heretofore  made  in  mining  for  these  metalo. 

Accompanying  this  supplementary  report,  Prof.  Irving  has  furnished 
for  preservation,  a  transcript  of  notes  made  by  him  in  18T3,  on  the 
iron  ores  and  iron  mounds  at  and  near  Black  River  Falls,  in  Jackson 
county,  with  the  analyses  of  the  ores,  so  far  as  they  have  been  finished; 
these  are  to  be  used  in  compiling  a  final  report,  when  the  survey  in 
that  neighborhood  is  completed.  From  these  notes  it  appears  that 
there  are  no  less  than  nine  different  beds  of  iron  ore  interlaminated 
with  slates,  crossing  the  river  at  various  points,  within  a  distance  of 
less  than  two  miles,  and  that  there  are  seven  prominent  mounds,  con- 
sisting chiefly,  or  largely  of  iron  ores,  with  slates  and  quartz.  Seve- 
ral analyses  already  completed,  indicate  26  to  32  per  cent,  of  metallic 
iron,  associated  chiefly  with  silica.  The  slates  are  supposed  to  be  of 
Huronian  age,  resting  upon  gneissoid  granite  below,  and  covered  un- 
conformably  by  the  Potsdam  sandstone. 

There  are  indications  of  a  great  lapse  of  time,  and  of  very  conside- 
rable erosion  after  these  slates  were  hardened  into  rock  and  elevated 
to  their  present  position,  but  before  the  deposition  of  the  Potsdain 
sands.  Specimens  were  obtained  near  the  mouth  of  Snow  creek,  show- 
ing  the  junction  of  the  sandstone  with  the  Huronian  slaty  ore,  in  a 
very  interesting  manner;  some  of  the  horizontal  and  some  of  the  in- 
clined layers  being  seen  in  the  same  hand  specimen. 

These  notes  are  accompanied  by  a  map  showing  the  occurrence  of 
the  mounds,  and  another  showing  the  position  of  the  iron  beds  along 
the  river  above  the  falls,  with  diagrams  illustrating  the  same. 

Prof.  Irving's  party  took  the  field  in  the  latter  part  of  April,  and 
continued  until  the  portion  of  the  appropriation  allotted  to  this  ser- 


ANNUAL  REPORT  FOR  1874.  49 

vice  was  exhausted  in  September.  Some  work  had  previously  been 
done  near  Madison.  The  services  of  Mr.  E.  T.  Sweet  were  again  se- 
cured, and  proved  to  be  altogether  satisfactory.  On  the  26th  of  June 
the  party  had  reached  Lodi,  and  soon  after,  Portage,  where  Prof. 
James  II.  Eaton,  of  Beloit,  joined  it  in  the  explorations  of  the  quartz- 
ites  of  Columbia  county.  He  continued  with  the  party  until  near  the 
close  of  the  season.  At  Grand  Rapids  the  party  ha4  an  interview  with 
Prof.  Davenport  Fisher,  of  the  ISFaval  School  at  Annapolis,  who  had 
made  and  furnished  to  the  survey  an  analysis  of  the  kaolin  of  that 
place.  In  September  Prof.  Irving  and  Mr.  Strong  met  in  Jackson 
county,  and  by  conference,  were  enabled  to  determine  some  results 
beneficial  to  the  survey. 

Reference  to  the  report  of  Prof.  Irving,  herewith  submitted,  will 
show  the  progress  he  has  made,  and  the  results,  so  far  as  they  havo 
been  worked  up,  at  the  present  time.  In  this  report  will  be  found 
much  detailed  information  of  local  interest  and  importance,  regarding 
the  dip,  thickness  and  economic  value  of  the  several  rocks,  and  its 
publication  cannot  but  be  useful  to  the  citizens  of  the  state  as  well  as 
to  the  scientific  geologist.  With  the  aid  of  the  map  and  sections,  all 
these  details  may  be  clearly  understood,  even  by  persons  not  familiar 
with  the  science  of  geology  generally. 

The  interesting  fact  is  pointed  out  that  the  boundaries  of  the  prai- 
ries, as  laid  down  upon  the  government  plats,  correspond,  in  a  gene- 
ral way,  with  the  boundaries  of  the  geological  formations  —  another 
instance  of  the  bearing  one  study  may  have  upon  another.  The  na- 
ture of  the  soil,  derived  directly  from  the  rocks,  has  much  to  do  with 
the  distribution  of  trees  and  other  plants  over  the  earth's  surface,  and 
hence  we  find  the  native  flora  considerably  modified  by  the  rocks  of 
the  several  geological  districts. 

The  artesian  well  at  the  state  house,  Madison,  disclosed  the  Arch- 
aean character  of  the  rock  immediately  below  the  Potsdam  at  that 
place,  and  gives  probability  to  the  suggestion  that  our  whole  state  is 
underlaid  by  these  rocks  at  no  great  depth. 
Wis.  SUB.— 4 


-  .    ,>   ii    A   Li  Y 

UNIVERSITY   OF 

CALIFORNIA. 


50  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

REGISTER  OF  THE  ARTESIAN  WELL  IN  THE  CAPITOL  PARK,  MADISON. 


*o    • 

2* 

j§s 

oj 

o 

*| 

fIL 

2& 

1 

P 

jp 

SOIL. 

926 

Top  of  well                              

348 

918 

8 

8 

340 

DRIFT. 

858 

60 

68 

280 

846 

12 

80 

268 

8^9 

17 

97 

251 

824 
804 

Grayish-brown  rock  (boulder  ^)  

5 

20 

102 
122 

246 
226 

Indurated  clay  (quite  compact)  

800 

Rock  (boulder9)  

4 

126 

222 

POTSDAM  SANDSTONE.* 

745 

Sandstone  gravel,  quite  loose,  white  and  yellow,  no  ce- 

55 

181 

167 

671 

Loose,  white,  uncemented  sand,  with  layers  of  yellow 

sand  ••  •  

74 

255 

93 

661 

Bottom  of  tubing  

10 

265 

83 

166 

White  sandrock,  grains  sharp,  but  always  somewhat 

rounded,  with  occasional  layers  of  grayish  color,  the 

whole  cemented  sufficiently  to  preserve  the  sides  of 

the  well.    Sample  from  700  feet  below  surface  showed 
under  microscope  very  much  rounded  grains  of  limp- 

id quartz,  some  perfectly  pure,  some  stained  in  spots 
with  oxide  of  iron  

495 

760 

—412 

131 

White  quartz  sandrock  of  finer  grain,  mixed  with  a  sub- 
stance resembling  porcelain  

35 

795 

—447 

122 

Red  clay-like  powder,  very  slightly  gritty,  under  high- 

est power  appears  to  be  mostly  very  fine  quartz  sand. 

9 

804 

—456 

120£ 

Coarse,  dark,  reddish-  brown  powder,  mostly  very  much 

rounded  quartz  grains,  but  mingled  with  some  dark, 

opaque  grains  also  rounded,  belonging  therefore  with 

iy 

805% 

—  457J 

ARCHAEAN. 

98 

Dark  grayish  mixed  rock,  very  hard  to  drill,  coming  up 
in  quite  large  fragments  all  angular;  carries  patches 
of  a  greenish  cleavable  mineral;  sp.  gr.  of  rock,  2.76; 

hardness,  5;  fuses  at  about  3  to  a  black  bead.    The 

included  mineral  (prehnite)  is  cleavable  and  semi- 

translucent,  and  fusible  at  3.5  to  4  to  a  white  enamel. 

22^ 

828 

^80 

89 

187 

1015 

—667 

The  numerous  artesian  wells,  though  not  always  successful  in 
affording  water,  show  very  important  results  in  regard  to  the  rock 
strata  far  beneath  the  surface.  The  recent  discovery  of  native  copper 
and  silver  in  the  well  at  Kilbourn  City,  at  the  depth  of  516  feet, 

*  Possibly  this  should  stand  next  before  the  gravel,  depth  80  feet. 


ANXUAL  REPORT  FOR  1874.  51 

must  be  deemed  one  of  no  inconsiderable  interest,  being  the  first  in- 
dication of  the  existence  of  these  metals  (imcombined)  in  the  central 
or  southern  part  of  the  state.  Whether  they  exist  at  this  place  in 
quantity  sufficient  to  be  profitably  mined  can  only  be  determined  by 
sinking  a  shaft  to  the  depth  indicated.  The  copper-bearing  rock  was 
exceedingly  hard,  and  had  a  depth  of  eighteen  feet.  Until  we  know 
the  dip  of  this  rock,  it  will  be  impossible  to  ascertain  its  real  thick- 
ness; if  the  stratum  lies  horizontally  (which  is  not  very  probable),  it 
has  a  thickness  of  eighteen  feet;  if  it  has  a  dip  of  4:5°  or  more,  its 
thickness  is  only  thirteen  feet  or  less.  It  is  not  improbable  that 
when  the  proper  trend  of  these  rocks  can  be  found,  a  search  in  the 
right  places  may  lead  to  further  discoveries  of  importance.  The  top 
of  this  well  is  347  feet  above  Lake  Michigan ;  Archaean  rocks  were 
reached  at  118  feet  below;  total  depth  of  the  well  (December,  1874) 
840  feet. 

One  of  the  first  results  of  Prof.  Irving's  survey  of  Dane  county 
was  the  identification  of  a  hitherto  unrecognized  layer  of  sandstone, 
far  down  in  what  has  been  classed  as  Lower  Magnesian  limestone; 
to  this,  in  accordance  with  the  custom  of  geologists,  he  has  given  the 
local  name  of  "  Madison  Sandstone."  It  is  much  used  in  and  about 
Madison  as  a  building  stone.  That  portion  of  the  Calciferous  or 
Lower  Magnesian  limestone  series  lying  below  the  Madison  Sand- 
stone, and  down  to  the  Potsdam,  forms  the  immediate  shore  of  Lake 
Mendota  (4th  lake),  and  has  with  much  propriety  been  named  the 
"  Mendota  Limestone  "  in  the  report.  This  explains  some  anamolous 
sections  heretofore  made,  and  introduces  two  new  names  into  the  local 
geological  nomenclature. 

We  thus  find  additional  resemblance  between  the  formations  in 
Wisconsin  and  those  in  Missouri,  where  Prof.  G.  C.  Swallow  long  ago 
recognized,  and  arranged  under  the  head  of  "  Calciferous  sandstone 
or  Magnesian  limestone  series,"  seven  different  members,  which  may 
now  be  parallelized  with  our  strata  as  follows: 

MISSOURI.  WISCONSIN. 

First  Limestone,  190  feet.  Buff  Limestone,  50  feet. 

Saccharoidal  Sandstone,  125  feet.  St.  Peters  Sandstone,  100  feet. 

Second  Limestone,  230  feet.  Main  Beds,  80  feet. 

Second  Sandstone,  70  feet.  Wanting. 

Third  Limestone,  350  feet.  Wanting. 

Third  Sandstone,  50  feet.  Madison  Sandstone,  35  feet. 

Fourth  Limestone,  300  feet.  Mendota  Limestone,  30  feet. 

Potsdam  Sandstone.  Potsdam  Sandstone. 

PROF.  T.  C.  CHAHBERLIN'S  PARTY. — Before  entering  upon  the  field 
work,  Prof.  Chamberlin  completed  his  report  of  the  work  done  in 


52  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

1873,  by  sending  a  supplementary  report,  which,  as  above  explained, 
could  not  be  prepared  in  time  to  be  bound  with  the  matter  previously 
reported  by  him.  This  supplementary  matter  is  therefore  herewith 
submitted,  and  will  be  restored  to  its  proper  place  in  the  preparation 
of  the  final  report,  as  contemplated  by  section  five  of  the  law  author- 
izing the  survey. 

In  this  report  will  be  found  many  details  with  respect  to  the  Lower 
Magnesian  limestone,  as  it  occurs  in  the  northeastern  part  of  the 
state,  showing  much  the  same  general  characteristics  as  in  the  south- 
western counties.  It  is  interesting  to  note  the  occurrence  of  a  con- 
siderable fault  in  the  strata  in  the  town  of  Ellington  (T.  22,  R.  16  E.), 
such  dislocations  being  rare  in  Wisconsin.  To  this  we  may  attribute 
some  very  marked  peculiarities  in  the  hydrography  of  that  vicinity. 
Wherever  mining  has  been  prosecuted  in  search  of  gold,  silver, 
copper,  etc.,  examination  of  the  rocks  gave  little  indication  of  the 
presence  of  these  metals;  and  it  has  very  often  been  the  business  of 
the  survey  to  discourage  the  search  for  ores  in  places  where  they  are 
not  to  be  found.  Copper-mining  at  Berlin  and  gold-mining  at  Win- 
neconne  are  among  the  projects  thus  discouraged. 

The  quartzites  of  Portland,  Dodge  county,  and  some  new  localities 
discovered  in  adjacent  portions  of  Jefferson  county,  are  fully  de- 
scribed. Several  other  outcrops  of  Archaean  rocks  are  described  —  as 
at  Berlin,  Mukwa  and  Keshena. 

The  important  subject  of  artesian  wells  is  also  fully  discussed  in 
this  report,  giving  many  details  that  will  be  of  great  value  in  the  fu- 
ture operations  of  well- digging. 

It  was  deemed  most  conducive  to  the  public  interest  to  direct  Prof. 
Chamberlin  to  continue  his  survey  from  Beloit  along  and  near  the 
south  line  of  the  state  to  Lake  Michigan,  and  thence  northward  be- 
tween his  line  of  operations  in  1873  and  the  shore  of  the  lake.  Though 
much  covered  with  drift,  it  was  hoped  that  a  sufficient  number  of  out- 
crops of  rock  could  be  found  to  reveal  the  general  geological  charac- 
ter of  this  district,  and  perhaps  develop  some  new  and  interesting  facts 
in  regard  to  this  portion  of  the  state.  Eunds  were  supplied  him  for 
expenses  of  the  field-work  on  the  first  of  May,  and  the  work  com- 
menced soon  afterwards.  By  the  last  of  August  this  party  was  able 
to  reach  the  extremity  of  the  peninsula  between  Lake  Michigan  and 
Green  Bay,  at  "  Death's  Door,"  and  to  commence  the  return  trip,  in 
which  some  points  of  special  interest  were  reexamined,  and  many  new 
localities  visited.  Active  duties  in  the  field  were  brought  to  a  close 
in  October.  The  services  of  Messrs.  L.  C.  Wooster,  G.  D.  Swezey, 
and  J.  H.  Chamberlin  were  secured  during,  portions  of  the  season; 


ANNUAL  KEPORT  FOR  1874.  53 

and  Mr.  F.  II.  King  was  engaged  to  continue  his  observations  upon 
animal  and  vegetable  life,  such  as  are  required  by  the  provisions  of 
the  law  authorizing  the  survey.  Two  thousand  five  hundred  miles  of 
travel  with  a  team ;  seven  thousand  specimens  of  rocks,  fossils,  and 
minerals  collected;  these  are  justly  deemed  a  good  season's  work. 

Prof.  Chamberlin's  report  of  his  operations  during  the  year  1874 
will  be  found  to  contain  ample  details  of  the  geology  of  the  district 
assigned  to  him.  These  will  settle  many  questions  as  to  the  non- 
occurrence  of  coal  and  other  useful  minerals,  which  are  dependent  up- 
on the  kind  of  rock  found.  The  difficulty  of  determining  the  proper 
order  of  succession  of  the  various  strata,  with  their  general  dip  and 
strike  in  a  region  where  outcrops  can  be  only  here  and  there  exam- 
ined, is  very  great.  Hence,  perhaps  there  may  still  remain  some  im- 
portant questions  for  future  investigation;  but  sufficient  has  been 
ascertained,  it  is  believed,  to  answer  all  the  general  objects  and  pur- 
poses of  this  survey. 

Attention  is  called,  in  this  report,  to  the  great  valley  diverging 
from  the  west  shore  of  Lake  Michigan  towards  the  southwest,  well 
marked  by  the  waters  of  Green  Bay,  Lake  Winnebago  and  the  valley 
of  Rock  river;  the  rock  ridge  bordering  this  great  ancient  valley  on 
the  east;  the  very  remarkable  drift  ridge,  locally  known  as  the  potash 
kettles,  extending  from  the  south  line  of  the  state  to  the  peninsula 
of  Green  Bay;  the  several  systems  of  parallel  drift  ridges,  some  of 
them  sharp  and  narrow,  called  hog's  backs;  and  the  more  level  dis- 
tricts along  the  immediate  shore  of  the  lake. 

A  very  important  and  interesting  deduction  made  by  Prof.  Cham- 
berlin,  as  a  result  of  his  explorations,  is  the  fiord  character  of  the 
peninsula  of  Green  Bay;  this  being  the  result  of  intense  glacial  ac- 
tion, perhaps  near  the  close  of  the  great  ice  period.  The  glacier 
seems  to  have  been  concentrated  upon  Lake  Superior  by  the  converg- 
ing shore  lines,  and  passing  southward  to  Green  Bay,  was  thence  di- 
verted towards  the  southeast,  plowing  six  or  more  great  furrows, 
which  are  now  indicated  by  bays  on  both  sides  of  the  peninsula. 
These  valleys,  or  fiords,  are  continuous  across  this  narrow  neck  of 
land,  and  may  be  traced  on  the  charts  of  the  lake  survey  upon  the 
bottom  of  Lake  Michigan,  for  a  distance  of  twelve  or  fourteen  miles. 
If  the  peninsula  north  of  Sturgeon  Bay  was  ever  covered  with 
drift,  it  has  been  entirely  removed,  perhaps  by  the  abrading  action  of 
waves  at  a  time  when  Lake  Michigan  stood  at  a  much  higher  level 
than  now ;  the  rock  surface  being  now  covered  only  with  a  thin  layer 
of  soil,  destitute  of  drift  material. 

Some  very  remarkable  facts  relating  to  the  course  of  streams  are 


54  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

referred  to  as  indicating  changes  that  have  taken  place  in  the  condi- 
tion of  the  land  in  remote  times. 

The  drainage  is  shown  to  be  a  proper  medium  between  the  slow- 
flowing  streams  and  swamps  of  a  flat  country,  requiring  artificial 
drainage,  and  the  rapid  currents  of  highly  inclined  lands,  causing  ex- 
tensive erosions  and  the  loss  of  the  more  fertile  portions  of  the  soil. 
Attention  is  given  to  the  fact  that  large  areas  represented  as  marsh 
on  the  government  plats  are  now  dry  and  arable;  that  many  of  the 
streams  have  disappeared  and  become  mere  periodical  runs;  and  that 
the  volume  of  running  water  has  been  considerably  reduced;  facts 
undoubtedly  due  to  the  removal  of  the  forests  and  the  cultivation  of 
the  soil. 

Prof.  Chamberlin,  with  the  active  and  intelligent  aid  of  Mr.  Swe- 
zey,  enters  with  much  detail  into  the  important  subject  of  the  distribu- 
tion of  plants  over  the  surface  of  the  state,  and  accompanies  his  report 
with  a  map  representing,  as  well  as  can  be  done,  the  principal  facts  as 
observed  and  recorded  during  the  progress  of  the  survey.  Plants  are 
arranged  into  fifteen  different  classes  or  groups,  each  of  which  occu- 
pies certain  localities  to  the  exclusion  of  the  others,  and  each  indicat- 
ing some  peculiarity  of  soil,  geological  formation,  or  climate. 

Under  the  head  of  Surface  Geology  will  be  found  many  important 
facts  in  regard  to  the  soil  and  subsoils,  of  which  he  distinguishes 
eight  different  kinds,  each  with  its  peculiar  qualities  and  value.  One 
of  these  —  the  calcareous  sandy  soil,  found  near  Elkhart  lake  —  con- 
sists mainly  of  small  crystals  of  dolomite  or  magnesian  limestone, 
which,  while  having  the  appearance  of  being  sandy  and  unpromising, 
is  found  to  possess  great  fertility. 

The  measurements  along  the  west  shore  of  Lake  Michigan,  intend- 
ed to  show  the  progress  that  lake  is  making  in  wearing  away  its 
banks,  are  not  only  of  interest  and  importance  at  the  present  time, 
but  will  possess  value  to  those  who  shall  come  after  us  for  many  years 
in  the  distant  future.  They  show  a  mean  annual  abrasion  in  Racine 
county  of  3.33  feet;  and  in  Milwaukee  county  of  2.77  feet.  The 
rapidity  of  geological  changes,  made  under  our  own  eyes,  is  promi- 
nently exhibited  in  the  fact  above  mentioned  of  a  ravine  having  been 
formed  near  Racine  within  the  past  twenty-eight  years,  which  is  half  a 
mile  in  length,  one  hundred  and  twenty  feet  wide  and  forty  feet  deep. 

The  ample  topographical  details,  including  lists  of  elevations,  will 
have  their  use  in  all  future  projects  for  the  construction  of  canals, 
railroads,  and  for  many  other  practical  and  useful  purposes. 

Section  two  of  the  act  to  provide  for  the  geological  survey,  among 
other  objects  and  duties,  very  properly  requires  observations  to  be 


ANNUAL  REPORT  FOR  1874.  55 

made  upon  the  animal  and  vegetable  productions  of  the  state,  with 
reference  to  its  agricultural  interests.  This  duty  has  been  assigned 
to  Mr.  F.  H.  King,  under  the  direction  of  Prof.  T.  C.  Chamberlin, 
one  of  the  assistants  in  the  survey.  Though  this  work  is  incomplete, 
it  is  deemed  best  to  present  herewith,  for  preservation  and  future  use 
the  two  reports  now  prepared  by  Mr.  King,  which  will  be  found  to 
contain  brief  notes  of  very  numerous  and  important  observations 
made  by  him  during  the  years  1873  and  1874,  relating  to  the  birds 
and  to  the  Lepidopterous  insects  of  the  state. 

The  notes  upon  the  birds  relate  chiefly  to  their  food,  as  ascertained 
by  an  examination  of  the  contents  of  the  stomach  of  the  several  spe- 
cies; this  becomes  important  by  showing  whether  they  destroy  our 
insect  enemies  or  friends.  It  is  only  by  such  observations,  made  by 
persons  who  find  pleasure  in  the  pursuit,  and  who  are  to  be  relied 
upon  for  care  and  accuracy,  that  the  truths  of  natural  history  can  be 
ascertained  and  recorded.  One  hundred  and  two  species  of  Wiscon- 
sin birds  are  mentioned,  and  facts  of  greater  or  less  importance  are 
recorded  in  regard  to  them.  Fifty-four  species  of  insects,  injurious 
to  one  hundred  and  twenty-six  species  of  plants,  and  seven  species 
whose  habits  are  such  as  to  be  deemed  beneficial,  are  included  in  this 
report. 

Mr.  King's  notes  are  to  be  preserved  for  use  in  making  up  a  more 
general  and  complete  work  upon  the  animal  and  vegetable  produc- 
tions of  the  state,  which  will  embrace  also  such  further  observations 
as  may  hereafter  be  made  during  the  continuance  of  the  survey. 

MR.  MOSES  STEONG'S  PAKTY. — As  early  in  the  season  of  1874  as 
the  weather  became  suitable  for  active  operations  in  the  field,  Mr. 
Strong,  with  the  aid  of  Mr.  George  Haven  as  an  assistant,  and  John 
Cain  as  teamster,  resumed  the  work  of  surveying  those  portions  of  the 
lead  region  not  covered  by  him  in  1873.  The  preceding  winter  bad 
been  spent  in  preparing  plats  and  collecting  such  information  of  the 
country  to  be  examined,  as  would  facilitate  the  field-work  of  the  sea- 
son. The  southern  and  eastern  portions  of  the  lead  region  were  first 
surveyed,  including  the  whole  of  Green  county;  and,  after  completing 
a  few  townships  in  the  northeastern  part  of  Iowa  county,  he  proceed- 
ed in  August  to  carry  out  that  portion  of  his  instructions  that  con- 
templated the  extension  of  his  survey  northward,  through  Bichland, 
Yernon  and  Monroe  counties  to  the  southern  limits  of  the  Archaean 
rocks  in  Jackson  county.  The  northern  portion  of  the  lead  region, 
and  the  much  broken  district  extending  from  the  great  east  and  west 
watershed  to  the  Wisconsin  river,  were  next  examined  in  detail. 


56  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

He  was  thus  fortunately  able  to  accomplish  the  whole  of  the  work 
assigned  to  him  at  the  beginning  of  the  season,  and  to  prepare  his 
second  annual  report,  with  the  necessary  maps,  sections  and  diagrams, 
within  the  time  prescribed  by  law. 

The  work  of  the  past  season  is  so  intimately  connected  with  that  of 
the  previous  year,  that  it  was  deemed  best  to  include  the  whole  in 
one  report ;  accordingly  this  has  been  done  by  Mr.  Strong,  so  that  the 
accompanying  report  gives  one  connected  and  comprehensive  view  of 
his  work,  and  its  results  up  to  the  present  time. 

In  this  report  will  be  found  full  details  with  respect  to  the  district 
thus  surveyed,  arranged  under  the  following  heads: 
Previous  publications  and  surveys ; 
Topographical  and  geological  maps  and  sections; 
Barometrical  observations; 
Physical  geography,  and  surface  geology; 
The  several  rock  formations;  being  the 
Potsdam  sandstone, 
Lower  Magnesian  limestone, 
St.  Peters  sandstone, 
Bufi'  and  Blue  (Trenton)  limestone, 
Galena  limestone,  and 
Cincinnati  group, 

All  considered  with  respect  to   their  geographical  boundaries,  litho- 
logical  character,  ores,  minerals  and  paleontology; 
The  origin  of  river  valleys ; 
Explanation  of  mining  terms; 
Present  condition  of  the  mines; 
Statistics  of  lead,  zinc  and  copper  production; 
Explorations  north  of  the  Wisconsin  river,  and 
Prehistoric  mounds  of  the  lead  region. 

Topographical  maps  accompany  this  report,  embracing  the  entire 
lead  region,  on  a  scale  of  one  mile  to  an  inch,  which  is  sufficient  to 
exhibit,  by  contour  lines  fifty  feet  apart  (vertically),  the  elevation  of 
every  point  above  the  level  of  the  sea.  These  maps  also  show  the  posi- 
tion of  the  public  roads.  Such  maps  have  special  value  not  only  in 
respect  to  future  railroad  surveys,  showing  at  once  the  practicability 
or  impracticability  of  any  contemplated  route,  and  thus  save  the  time 
and  expense  of  a  very  large  amount  of  preliminary  surveys,  but  are, 
obviously,  of  great  importance  to  the  mining  interest,  as  indicating 
the  proper  system  of  drainage,  location  of  "levels,"  etc.  Geological 
maps  are  also  furnished,  constructed  upon  the  same  scale,  showing  the 
position  of  the  several  rock  formations,  by  which  the  relation  of  a  ly 


ANNUAL  REPORT  FOR  1874.  57 

particular  quarter  section  of  land  to  these  formations  can  be  seen,  and 
its  value  with,  respect  to  mining  prospects  at  once  ascertained.  The 
information  from  which  these  maps  were  constructed  has  been  col- 
lected with  great  care,  involving  an  immense  number  of  barometrical 
observations,  and  a  great  many  miles  travel. 

From  information  contained  in  these  two  series  of  maps,  it  is  easy  to 
construct  geological  sections  on  any  desired  Une.  Those  prepared  by 
Mr.  Strong,  and  accompanying  his  report,  have  been  selected  with  a  view 
of  showing  the  "  dip,  number,  magnitude,  order  and  relative  position 
of  the  various  strata,"  as  well  as  the  amount  of  denudation  to  which 
the  country  has  been  subjected.  The  amount  of  denudation  thus 
shown,  seems  wonderful,  but  is  accounted  for  when  we  consider  the 
immense  time  during  which  the  rocks  have  been  exposed  to  the  abrad- 
ing influences;  being  no  less  than  the  time  occupied  by  the  formation 
of  the  Devonian,  Carboniferous,  and  all  subsequently  deposited  rocks. 

The  regularity  and  simplicity  of  the  geological  features  of  the  lead 
region  are  quite  remarkable;  there  being  no  sudden  breaks  or  "  faults  " 
in  the  strata,  no  upheavals  to  any  considerable  extent;  no  intrusive 
rocks,  breaking  through  the  different  formations;  and  the  veins  from 
which  ores  are  extracted  do  not  penetrate  the  strata  below  the  horizon 
of  the  St.  Peters  sandstone. 

The  origin  and  nature  of  springs  are  not  well  understood,  many 
crude  notions  being  commonly  entertained  in  regard  to  them;  hence 
Mr.  Strong  has,  very  properly,  adduced  the  facts  to  show  that  the 
springs  near  the  top  of  the  Blue  Mounds  have  an  abundant  source  of 
supply,  even  in  the  small  area  of  the  mound  above. 

Though  the  lead  region  is  supposed  to  have  been  exempt  from  the 
influence  of  the  glaciers  which  have  distributed  so  much  drift  mate- 

O 

rial  over  adjacent  districts,  there  are  some  facts  still  requiring  explan- 
ation, particularly  the  one  first  noticed  by  Prof.  Whitney,  of  the  occur- 
rence of  blocks  of  St.  Peters  sandstone  resting  upon  formations  of 
later  age.  The  boundary  of  the  glacial  drift  through  Green  county 
has  now  been  accurately  traced.  The  occurrence  of  drift  material  in 
the  valleys  of  the  Mississippi  and  lower  Wisconsin  is  rightly  attrib- 
uted to  river  transportation  from  above. 

With  respect  to  the  several  geological  formations,  much  informa- 
tion is  given  in  detail,  systematically  arranged,  and  not  before  pub- 
lished. 

Mr.  Strong's  survey,  and  the  experience  of  the  past  twelve  years 
have  given  additional  proof  of  the  correctness  of  the  views  of  Prof. 
J.  D.  Whitney,  as  set  forth  in  his  report,  published  in  1861.  Among 
the  most  important  of  these  views  are  the  following: 


58  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

That  the  lead  crevices,  with  their  mineral  contents,  are  not  true 
veins  extending  indefinitely  downwards,  but  partake  of  the  nature  of 
shrinkage  cracks  or  joints,  such  as  may  be  seen  in  almost  all  lime- 
stone quarries. 

That  though  the  mineral  grounds  have  considerable  lateral  extent, 
they  reach  only  a  short  distance  downwards. 

That  the  filling  of  the  crevices  with  mineral  matter  was  not  from 
below  by  volcanic  heat,  but  from  above,  and  by  precipitation  from  a 
solution. 

Much  doubt  and  uncertainty  still  exist  as  to  the  origin  of  the 
metallic  sulphurets,  and  as  to  the  time  when,  and  the  special  condi- 
tions under  which  they  were  introduced  into  these  crevice  joints.  The 
occurence  of  a  similar  lead  region  in  southeastern  Missouri,  and  of 
another  in  the  southwest  part  of  the  same  state ;  the  first  in  the  Lower 
Magnesian  limestone,  the  last  in  rocks  of  the  Subcarboniferous  age, 
would  seem  to  indicate  either  that  these  conditions  were  repeated  at 
three  different  times,  or  that  they  wrere  brought  about  at  a  time  sub- 
sequent to  the  deposition  of  the  Subcarboniferous  limestones. 

Attention  is  directed  to  the  fact  that  the  valley  of  Sugar  river, 
which  constitutes  the  eastern  boundary  of  the  lead  region,  is  much 
broader  and  deeper  in  proportion  to  the  amount  of  water  at  present 
flowing  in  that  stream  than  is  usual;  and  hence  the  inference  that  at 
some  time  in  the  remote  past,  a  large  river  found  its  channel  along  the 
course  of  the  present  Sugar  river.  With  a  breadth  of  stream  of  only 
about  one  hundred  feet,  it  has  a  valley  as  broad  as  that  of  the  Missis- 
sippi. In  the  future  progress  of  the  survey,  additional  light  may  be 
thrown  upon  this  subject. 

The  information  contained  in  this  report  with  respect  to  the  pres- 
ent condition  of  the  mines  will  have  a  practical  value,  and  will  con- 
tribute much  towards  directing  the  attention  of  capital  and  enterprise 
to  that  important  industrial  interest  in  our  state. 


ANNUAL  REPORT  FOR  1874. 


59 


The  following  table  shows  the  amount  of  lead  and  zinc  produced  for 
the  years  named: 


LEAD. 

ZIKC 

YEARS. 

Galenite, 
Pounds. 

Smithsonite, 
Pounds. 

Blende, 
Pounds. 

1860  .. 

320,000 

1861  

266  000 

1862  

17  037  912 

1863  

15  105  577 

1  120  000 

1864  

13  014  201 

3  173  333 

1865  

14  337  895 

4  198,200 

1866  

14  029,192 

7,373,333 

1867  

13  820  784 

5  181  445 

841,310 

1868  

13,  869,  619 

4,302,383 

3,078,435 

1*69  

13  426  721 

4,547,971 

6,252,420 

1870  

13,754  159 

4,429,585 

7,  414,  022 

1871  

13  484  ?10 

16  618  160 

9,303,625 

1872  

11  622  668 

27,021,388 

16,256,970 

1873  

9  919  734 

18  528  906 

15,074,664 

Total  

163  422,672 

97,080,704 

58,221,446 

It  will  be  seen  from  the  above  that  while  the  production  of  lead  ore 
has  been  diminishing,  during  the  past  three  or  four  years,  that  of  zinc 
ores  is  rapidly  increasing. 

The  explorations  made  north  of  the  Wisconsin  river,  and  outside  of 
the  lead  region  proper,  were  necessarily  of  a  more  general  character, 
and  the  facts  collected  are  represented  upon  maps  on  a  much  smaller 
scale.  Those  made  in  1874  were  confined  chiefly  to  a  single  range 
(range  two  west)  of  townships,  so  that  the  entire  extent  of  the 
Paleozoic  rocks  could  be  explored  within  the  time  and  means  appli- 
cable to  this  portion  of  the  work.  The  most  northern  outlier  of  the 
St.  Peters  sandstone  was  found  in  the  south  part  of  township  twelve; 
and  the  last  occurrence  of  limestone  (Lower  Magnesian)  in  this  range 
is  on  sections  10  and  15  in  township  seventeen. 

Here  are  found  those  high,  continuous  dividing  ridges  forming  seri- 
ous obstacles  to  railroad  construction,  and  from  which  fine  views  of 
the  surrounding  valleys  may  be  seen. 

The  search  for  oil  at  "  Oil  City  "  resulted  only  in  a  fine  flowing  ar- 
tesian well  whose  waters  may  be  found  to  possess  medicinal  virtues,  and 
a  knowledge  of  the  strata  below,  down  to  the  Archaean  rocks.  Here 
the  Potsdam  sandstone  has  the  unusual  thickness  of  8-M  feet. 

These  explorations,  being  in  a  line  nearly  parallel  with  the  Missis- 
sippi river,  will  form  a  convenient  base  for  the  surveys  to  be  made  in 
1875,  between  that  line  and  the  river. 


60  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

The  ancient  artificial  mounds,  especially  those  of  imitative  forms, 
found  within  the  district  surveyed  by  Mr.  Strong,  have  received  a 
share  of  his  attention.  They  were  built  in  prehistoric  times,  by  an 
extinct  race  of  people,  whose  existence  here  is  believed  to  have  been 
with  that  of  the  Mastodon.  They  thus  form  the  connecting  coeval 
link  between  the  geologist  and  antiquary;  the  duties  of  the  one  cease, 
while  those  of  the  other  commence  with  the  epoch  of  the  mound 
builders. 

SURVEYS  IN  OCONTO  COUNTY,  BY  MAJOR  T.  B.  BROOKS.  —  Maj. 
Brooks,  late  of  the  geological  survey  of  the  state  of  Michigan,  under- 
took to  trace  the  Iron-bearing,  and  other  rocks  found  on  the  east  side 
of  the  Menomonee  river  of  Green  Bay,  above  Sturgeon  Falls,  across 
that  river  into  Wisconsin,  and  to  ascertain  as  far  as  was  practicable 
their  southern  and  western  boundaries,  where  they  are  succeeded  by 
granitic  rocks.  Special  search  was  to  be  made  with  the  aid  of  the 
"  mining  compass  "  and  otherwise,  for  iron  ores,  but  the  money  ap- 
plicable to  this  survey  not  being  adequate  to  the  sinking  of  exper- 
imental pits,  shafts,  or  drifts,  such  work  was  necessarily  left  to  private 
enterprise,  guided  by  the  results  of  such  survey  as  he  should  be  able 
to  make.  A  suit  of  specimens  was  to  be  collected  and  forwarded  to 
the  chief  geologist,  with  a  full  report  in  detail,  illustrated  by  the  ne- 
cessary maps,  sections  and  diagrams.  All  chemical  analyses  were  to 
be  made  by  Prof.  Daniells,  of  Madison. 

Maj.  Brooks  commenced  active  operations  in  the  woods  witli 
ample  assistance  and  supplies,  on  the  10th  of  August,  and  the  work 
was  continued  fifty-six  days.  The  weather,  with  slight  exceptions, 
proved  favorable;  and  the  report  of  results  will  show  that  each  per- 
son engaged  must  have  done  his  whole  duty.  His  camps  were  moved 
along  the  course  of  the  river,  from  which  he  extended  his  observa- 
tions south  to  the  outcrops  of  the  granite,  and  west,  as  far  as  the 
"  Great  Swamp,"  in  range  17  E.,  town  40  1ST.  He  was  thus  able, 
though  not  without  much  exposure  and  difficulty,  to  accomplish  all 
the  objects  proposed,  and  in  a  satisfactory  manner. 

It  is  gratifying  to  know  that  his  report,  now  being  prepared,  will 
show  that  the  Iron  range  extends  across  the  Menomonee  into  Wis- 
consin, and  that  there  is  a  strong  probability  that  it  will  hereafter  be 
found  to  contain,  within  this  state,  workable  beds  of  ore. 

The  rocks  examined,  as  in  other  portions  of  the  Archaean  regions, 
were  found  to  be  quite  local  in  extent,  and  often  gradually  passing, 
by  insensible  degrees,  from  one  to  another,  rendering  it  very  difficult, 
if  not  impossible,  to  distinguish  the  different  kinds,  and  to  classify 


ANNUAL  REPORT  FOR  1874.  61 

them  under  appropriate  names.  Efforts  have  been  made  to  overcome 
this  difficulty  by  chemical  analysis,  and  also  by  microscopic  examina- 
tion of  very  thin  sections,  prepared  with  great  care  and  skill.  In  this 
way  it  is  sometimes  found  that  rocks,  having  the  same  general  ap- 
pearance to  the  eye,  are  made  up  by  the  aggregation  of  very  different 
minerals.  The  specimens  of  rocks  and  minerals  sent  in  were  col- 
lected and  transported  with  very  considerable  labor.  They  are  all 
numbered,  and  the  exact  locality  from  which  they  were  obtained  prop- 
erly designated.  They  will  be  of  much  use  in  the  further  prosecu- 
tion of  the  survey,  and  will,  at  its  close,  be  distributed  to  the  institu- 
tions entitled  to  receive  them  in^ accordance  with  the  law. 

One  of  the  most  serious  difficulties  met  with  by  Maj.  Brooks  and 
his  party,  and  which  materially  retarded  the  progress  of  his  work, 
arose  from  the  gross  inaccuracies  of  the  government  surveys  in  that 
part  of  the  state,  and  the  careless  and  insufficient  manner  in  which 
the  lines  and  corners  were  established.  Lakes  were  found  having  but 
little  resemblance  to  their  representation  upon  the  plats ;  streams  are 
made  to  run  where  none  exist;  swamps  are  laid  down  where  excellent 
pine-lands  yield  an  abundance  of  lumber;  when  a  tract  of  land  is 
"  entered,"  the  purchaser  may  find  his  quantity  or  number  of  acres 
deficient,  or  largely  in  excess.  It  is  matter  of  common  remark 
among  woodsmen  in  this  region,  that  the  Wisconsin  surveys  are 
much  less  reliable  than  those  of  Michigan  on  the  opposite  side  of  the 
river.  Under  these  circumstances,  it  may  be  a  question  whether  it  is 
not  the  duty  of  the  government  to  resurvey  in  a  more  thorough  and 
accurate  manner,  the  public  lands  in  this  region  of  the  country  before 
they  become  of  so  much  value  as  to  lead  to  endless  trouble  in  attempt- 
ing to  retrace  the  section  lines. 

It  is  much  to  be  regretted  that  the  several  stations  of  the  United 
States  lake  survey  were  not  connected  with  the  lines  of  the  public 
land  survey.  This  would  have  afforded  many  points  for  correcting  the 
maps  projected  from  the  land  surveys  alone. 

At  the  suggestion  of  the  geological  survey,  Gen.  A.  A.  Humph- 
rys,  Chief  of  Engineers,  directed  that  the  latitude  and  longitude  of 
certain  points  upon  the  fourth  principal  meridian,  the  base,  and  the 
correction  lines,  be  ascertained  with  the  utmost  exactness.  These, 
being  the  governing  lines  of  the  land  surveys,  are  most  important; 
and  it  is,  therefore,  extremely  desirable  that  their  exact  position 
should  be  ascertained. 

As  the  first  fruit  of  this  application,  the  following  determinations 
were  furnished  to  the  survey  by  Gen.  C.  B.  Comstock,  on  the  17th 
of  July,  187-i: 


62  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

1.  Intersection  of  the  fourth  principal  meridian  with  the  state  line  between  Illinois 
and  Wisconsin,  lat.  42°  30'  26.1";  long.  90°  25'  33.6". 

2.  First  section  corner  of  the  Wisconsin  survey  on  the  state  line  west  of  the  fourth 
principal  meridian,  lat.  42°  30'  26.4";  long.  90°  26'  44.2". 

3.  Southeast  corner  of  section  13,  township  18,  range  1  west,  lat.  44°  1'  49.6";  long. 
90°  25'  56". 

4.  Northeast  corner  of  section  1,  township  18,  range  1  west,  lat.  44°  4'  26.6";  long. 
90°  25'  56.7". 

5.  Southeast  corner  of  section  31,  township  21,  range  3  east,  lat.  44°  14'  57.3";  long. 
90°  10'  45.8". 

6.  Southwest  corner  of  section  31,  township  21,  range  3  east,  lat.  44°  14'  57.2";  long. 
90°  11'  48.9". 

Points  Nos.  5  and  6  are  on  the  correction  line  between  townships  20  and  21,  near 
Balch's  Ranch,  on  the  Wisconsin  Valley  Railroad. 

On  the  correction  line  between  townships  30  and  31,  range  19  west,  east  of  the  St. 
Croix  river. 

7.  Southeast  corner  of  section  34,  township  31,  range  19  west,  lat.  45°  7'  21.8";  long. 
92°  41'  24.6". 

8.  Southwest  corner  of  section  33,  township  31,  range  19  west,  lat.  45°  7'  22.1";  long. 
92°  43'  52.1". 

The  following  local  bearings  were  determined: 

1.  The  state  line  between  Illinois  and  Wisconsin,  from  its  intersection  with  the  fourth 
principal  meridian,  bears  W.  16'  17"  N.  to  point  No.  2  above. 

2.  The  fourth  principal  meridian,  from  the  southeast  corner  of  section  13,  township  18, 
range  1  west,  bears  N.  11'  10"  W.  to  point  No.  4  above. 

3.  The  correction  line  between  townships  20  and  21,  from  the  southeast  corner  of  sec- 
tion 31,  township  21,  range  3  east,  bears  W.  5'  18"  S.  to  point  No.  6  above. 

4.  The  correction  line  between  townships  30  and  31,  from  the  southeast  corner  of  sec- 
tion 34,  bears  W.  10'  20"  N.  to  point  No.  8  above. 

In  accordance  with  an  act  of  congress,  and  upon  application  from 
the  state  geological  survey,  as  explained  in  my  last  report,  the  super- 
intendent of  the  coast  survey  has  made  arrangements  for  the  prosecu- 
tion, with  suitable  instruments,  of  geodetic  surveys  within  this  state. 
These  will  consist  of  the  determination,  by  the  accurate  methods  of 
that  survey,  of  the  geographical  position  of  certain  prominent  points, 
and  the  measurement  of  a  base  line,  from  which,  by  a  connected  sys- 
tem of  triangles,  with  sides  ten  to  twenty  or  more  miles  in  length,  aa 
amount  of  exact  knowledge  of  the  geographical  and  topographical  fea- 
tures of  the  state  will  be  acquired,  sufficient  for  the  projection  of  a 
correct  map.  These  surveys  when  completed  and  properly  connected 
with  the  lines  of  the  land  survey  will  leave  nothing  to  be  desired. 

The  work  of  the  past  season  has  been  the  determination  of  the  lati- 
tude and  longitude  of  Madison  and  La  Crosse,  and  reconnoissance 
necessary  for  the  selection  of  suitable  triangulation  stations,  along  the 
valley  of  the  Wisconsin  river  from  Prairie  du  Chien  to  Kilbourn 
City.  This  important  survey  is  very  properly  placed  in  the  hands  of 


ANNUAL  REPORT  FOR  1874.  63 

Dr.  John  E.  Davies,  of  the  State  University,  and  affords  excellent  op- 
portunities for  giving  instruction  in  the  several  branches  of  knowledge 
required  for  such  work. 

Mr.  Frank  Ives,  having  spent  much  time  in  the  valley  of  the  Bois 
Brule  river,  Douglas  county,  with  his  attention  upon  the  geological 
features,  was  requested  to  make  a  report  of  the  results  of  his  observa- 
tions for  the  use  of  the  geological  survey.  A  copy  of  this  report  is 
herewith  submitted.  It  will  be  found  to  contain  much  local  infor- 
mation of  considerable  importance,  which  could  not  otherwise  have 
been  obtained  except  at  a  very  considerable  expense,  owing  to  the 
wildness  and  unsettled  condition  of  the  country. 

The  position  of  many  of  the  rapids,  falls,  and  lake-like  expansions 
of  the  river  is  here  first  ascertained ;  the  location  of  several,  before 
unknown,  outcrops  of  the  Lake  Superior  sandslone,  and  the  discovery 
of  a  range  of  possibly  mineral-bearing  trap  rocks,  in  the  south  part  of 
township  43,  range  10  west,  are  among  the  items  of  importance  in 
this  report.  Some  remarkable  drift  ridges,  extending  across  the  val- 
ley, seem  to  indicate  several  successive  stages  in  the  decay  of  the 
ancient  glaciers,  each  leaving  traces  of  its  work  in  the  form  of  ridges, 
resembling,  in  many  respects,  the  "  terminal  moraines  "  of  the  mod- 
ern glaciers  of  the  Alps.  Above  this  most  ancient  or  boulder  drift, 
Mr.  Ives  recognizes  two  distinct  epochs;  one  represented  by  the  sand 
and  fine  gravel  of  the  so  called  barrens;  the  other  by  the  red,  marly 
clay,  so  well  known  on  the  borders  of  Lake  Superior. 

His  observations  upon  the  soil,  climate  and  mineral  productions, 
seem  to  be  judicious  and  well  worthy  of  the  consideration  of  all  who 
are  interested  in  that  portion  of  our  state. 

Mr.  Gustavus  Bode  of  Milwaukee  has  furnished  the  survey  with 
the  analysis  of  ten  springs  and  wells,  made  during  the  past  year,  thus 
affording  additional  knowledge  of  the  character  of  the  natural  waters 
of  the  state.  Of  these,  eight  have  the  bicarbonates  of  lime  and 
magnesia  as  their  chief  ingredients,  supplied  directly  from  the  mag- 
nesian  limestones  abounding,  not  only  in  the  solid  rock,  but  in  the 
gravel  and  boulders  of  the  drift.  The  other  two  indicate  the  pres- 
ence of  sulphuric  acid,  arising  probably  from  the  decomposition  of 
iron  sulphurets,  by  which  these  salts  have  been  converted  into  sul- 
phates of  lime  and  magnesia.  They  also  contain  the  sulphate  of  soda. 
If  these  waters  could  be  examined  as  they  first  issue  from  the  ground, 
they  would,  doubtless,  show  the  presence  of  gaseous  matter  giving 
them  qualities  not  indicated  by  the  analysis  of  the  solid  substances 
obtained  by  evaporation.  Several  springs  and  wells  are  known  to  be 
highly  impregnated  with  sulphuretted  hydrogen,  and,  doubtless,  we 


64  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

have  many  waters  whose  medicinal  qualities  are  of  great  value,  but 
not  yet  known  and  appreciated. 

It  will  be  seen  that  the  work  of  the  several  parties  has  been  so  dis- 
tributed over  the  state  as  to  give  the  most  general  and  correct  view  of 
the  several  rock-formations,  and  prepare  the  way  for  greater  progress 
during  the  remainder  of  the  time  allotted  to  the  survey.  The  most 
recent  rocks  —  the  Drift,  Devonian  and  Upper  Silurian  came  under 
the  special  consideration  of  Prof.  Chamberlin ;  the  Lower  Silurian  of 
the  Lead  region  and  the  country  immediately  north  of  it  were  inves- 
tigated by  Mr.  Strong;  while  the  more  ancient  (Archaean)  has  chiefly 
received  the  attention  of  Prof.  Irving  and  Maj.  Brooks. 

The  chemical  analyses  needed  for  the  survey  have  been,  as  hereto- 
fore, under  the  direction  of  Prof.  W.  "W.  Daniells,  of  the  State  Uni- 
versity, who  has  made  a  great  number  of  full  analyses,  and  numerous 
examinations,  with  a  view  to  the  determination  of  the  value  of  cer- 
tain mineral  products. 

GENERAL  GEOLOGICAL  MAP.  —  With  this  report  is  presented  a  copy 
of  Mr.  Chapman's  sectional  map  of  the  state,  on  a  scale  of  six  miles 
to  an  inch,  upon  which  is  represented  the  geological  features  so  far  as 
they  are  known  up  to  the  date  of  this  report. 

LIST  OF  MAPS  AND  SECTIONS  ACCOMPANYING  THIS  REPORT. 

I.  PROF.  IRVING'S  SUPPLEMENTARY  REPORT,  1873. 

I.  General  Map  of  Northern  Wisconsin.    Plate  4. 

II.  Topographical  and  Outline  Map  of  the  Apostle  Islands.    Plate  5. 

III.  Additional  map  for  Plate  1  —  Ashland  county. 

IV.  Map  of  the  Ashland  Mining  Company's  Location.    Plate  8. 

V.    Showing  the  occurrence  of  the  Iron  Mounds,  in  the  vicinity  of  Black  River 

Falls.    Plate  6. 

VI.    Showing  the  Formations  in  detail  along  Black  river,  above  the  falls. 
Plate  7. 

II.  PROF.  IRVING'S  REPORT,  1874. 

VII.        Map  of  Townships  5,  6,  7  and  8,  in  Ranges  8,  9,  10  and  11. 
VIII.        Map  of  T.  9,  10, 11  and  12,  R.  8,  9,  10  and  11. 
IX.        Map  of  T.  13,  14,  15  and  16,  R.  8,  9,  10  and  11. 
X.        Map  of  T.  17,  18,  19  and  20,  R.  8,  9,  10  and  11. 
X.  (2)  Map  of  T.  21,  22,  23  and  24,  R,  7,  8,  9  and  10  E. 
X.  (3)  Map  of  T.  25,  26,  27,  28  and  29,  R.  5,  6,  7  and  8  E. 
X.  (4)  Map  of  T.  21,  22,  23  and  24,  R.  3,  4,  5  and  6  E. 
X.  (5)  Map  of  T.  21,  22,  23  and  24,  R.  1,  2,  3  and  4  W. 
XI.        Sections  in  central  Dane  county.    Plate  2. 

XII.        Grouped  sections  in  Dane  county.    (Double  sheet.)    Plates  3  and  4. 
XIII.        Sections  in  Dane  and  Columbia  counties. 


ANNUAL  REPORT  FOR  1874. 


65 


III.  PKOF.  CHAMBERLIK'S  REPORT,  1874. 

XIV.  Geological  Map,  T.  1,  2,  3  and  4,  R.  17,  18,  19  and  20. 

XV.  Geological  Map,  T.  1,  2,  3  and  4,  R.  21,  22  and  23. 

XVI.  Geological  Map,  T.  5,  6,  7  and  8,  R,  19,  20,  21,  22  and  23. 

XVII.  Topographical  Map  of  Milwaukee  county. 

XVIII.  Geological  Map,  T.  9,  10,  11  and  12,  R.  19,  20,  21  and  22. 

XIX.  "           "     T.  13,  14,  15  and  16,  R.  20,  21,  22  and  23. 

XX.  "           "     T.  17,  18,  19  and  20,  R.  21,  22,  23,  24  and  25. 

XXI.  "           "     T.  21,  22,  23  and  24,  R.  23,  24  and  25. 

XXII.  "           "     T.  21,  22,  23  and  24,  R.  19,  20,  21  and  22. 

XXIII.  "  "     T.  25,  26,  27  and  28,  R.  23,  24,  25,  26  and  27. 

XXIV.  Profile  of  Drift  Formations. 
XXV.  Map  of  Subsoils. 

XXVI.  Map  of  Post  Tertiary  and  Recent  Formations. 

IV.  MR.  STRONG'S  REPORT,  1874. 

XXVII.  Geological  Map,  T.  1  and  2,  R.  2  and  3  W. 

XXVIII.  Topographical  Map,  T.  1  and  2,  R.  2,  3  and  4  W. 

XXIX.  Geological  Map,  T.  1  and  2,  R.  1  E.  and  1  W. 

XXX.  Topographical  Map,  T.  1  and  2,  R.  1  E.  and  1  W. 

XXXI.  Geological  Map,  T.  1  and  2,  R.  4  and  5  E. 

XXXII.  Topographical  Map,  T.  1  and  2,  R.  4  and  5  E. 

XXXIII.  Geological  Map,  T.  1  and  2,  R.  6  and  7  E. 

XXXIV.  Topographical  Map,  T.  1  and  2,  R.  6  and  7  E. 
XXXV.  Geological  Map,  T.  1  and  2,  R.  8  and  9  E. 

XXXVI.  Topographical  Map,  T.  1  and  2,  R.  8  and  9  E. 

XXXVII.  Geological  Map,  T.  1,  R.  4,  5  and  6  W.,  and  T.  2,  R.  4  ^. 

XXXVIII.  Topographical  Map,  T.  3,  R.  4,  5  and  6  W. 

XXXIX.  Geological  Map,  T.  3,  R.  1,  2  and  3  W.  and  R.  1  E. 

XL.  Topographical  Map,  T.  3,  R.  1,  2  and  3  W.  and  R.  1  E. 

XLI.  Geological  Map,  T.  3,  R.  4  and  5  E. 

XLII.  Topographical  Map,  T.  3  and  4,  R.  4  and  5  E. 

XLIII.  Geological  Map,  T.  3  and  4,  R.  6  and  7,  E. 

XLIV.  Topographical  Map,  T.  3  and  4,  R.  6  and  7  E. 

XLV.  Geological  Map,  T.  3  and  4,  R.  8  and  9  E. 

XLVI.  Topographical  Map,  T.  3  and  4,  R.  8  and  9  E. 

XLVII.  Geological  Map,  T.  6,  R.  6  W. 

XL  VIII.  "           "      T.  6  and  7,  R.  4  and  5  W. 

XLIX.  "           "      T.  6  and  7,  R.  2  and  3  W. 

L.  "           "      T.  6  and  7,  R.  1  W.  and  1  E. 

LI.  "           "      T.  6,  7  and  8,  R.  4  E. 

LIL  "           "     T.  8,  R.  1,  2  and  3  W.  and  R.  1  E. 

LIII.  "           "      T.  8  to  22,  R.  2  W. 

LIV.  Profiles  (double  sheet). 
LIV.  (2)  Ancient  Mounds. 

LV.  General  Geological  Map  of  the  State,  in  four  sheets. 


ADDITIONS. 


XXIV.  (2)  Geological  Profiles. 
XXVI.  (2)  Map  of  Vegetation. 
;  XXVI.  (3)  Topographical  Map. 
Wis.  SUE.— 5 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


LIST  OF  PAPERS  ACCOMPANYING  THIS  REPORT. 

R.  D.  Irving's  Supplementary  Report. 

R.  D.  Irving's  Transcript  of  notes  relating  to  Black  River  Falls. 

R.  D.  Irving's  Report,  1874. 

T.  C,  Chamberlin's  Supplementary  Report. 

T.  C.  Chamberlin's  Report,  1874. 

F.  H.  King's  Report  on  Birds. 

F.  H.  King's  Report  on  Insects. 

Moses  Strong's  Report,  1874. 

Frank  Ives'  Report,  Douglas  County. 

J.  H.  Eaton's  Report,  Quaternary  of  Central  Wisconsin. 


EEPOET  OF  PEOGEESS  AND  EESTJLTS, 

FOR  THE  YEAR  1S75.1 


BY   O.   W.   WIGHT. 


In  compliance  with  a  requirement  of  the  act  "  to  provide  for  a  com- 
plete Geological  Survey  of  Wisconsin,"  approved  March  19,  1873,  I 
have  the  honor  to  report  the  progress  made  during  the  third  year  of 
the  survey. 

BRIEF  HISTORY  OF  PREVIOUS  GEOLOGICAL  SURVEYS  IN  WISCONSIN. — 
The  first  geological  survey  undertaken  by  the  government  of  the 
United  States  was  instituted  by  the  appointment  of  G.  W.  Feather- 
stonhaugh,  Esq.,  by  the  war  department,  with  instructions  to  make  a 
reconnoissance  "  of  the  elevated  region  lying  between  the  Missouri 
river  and  the  Red  river,  known  under  the  designation  of  the  Ozark 
mountains."  It  was  in  the  early  part  of  the  year  1834.  In  the  win- 
ter of  1834-35,  that  gentleman  visited  the  lead  mines  of  Missouri  and 
made  a  perfectly  worthless  report.  The  next  year  Mr.  Featherston- 
haugh  was  employed  by  the  government  under  the  title  of  United 
States  Geologist  to  explore  the  region  between  the  St.  Peters  river 
and  the  Missouri,  and  to  make  a  general  reconnoissance  of  the  north- 
west. He  referred  the  whole  series  of  Lower  Silurian  rocks  in  the  lead 
region  of  Wisconsin  and  up  the  river  to  the  falls  of  St.  Anthony  and 

1  The  fullest  opportunity  has  been  offered  the  author  of  this  report  to  revise  it  for  this 
volume,  but  not  having  been  accepted,  the  delicate  duty  has  devolved  upon  very  unwfl- 
ing  hands.  Certain  portions  of  an  annual  report  necessarily  refer  to  matters  of  transient 
importance  and  are  of  little  subsequent  value.  Such  portions  of  this  report  have  been 
omitted,  viz. :  A  financial  statement,  a  business  account  of  the  work  in  Oconto  county, 
and  an  outline  of  the  work  remaining  to  be  done.  The  law  authorizing  the  survey, 
which  has  been  previously  given,  and  the  reports  of  assistants  prepared  by  themselves, 
are  also  omitted,  as  in  the  case  of  the  reports  of  1873  and  1874.  I  have  deemed  myself 
under  obligations  to  publish  everything  of  a  geological  nature,  even  where  dissenting 
from  the  views  presented.  T.  C.  C. 


68  GEOLOGICAL  SURVEY  OF  WISCONSIN.  v 

beyond  to  the  carboniferous  limestone.  It  is  hardly  possible  to 
conceive  of  a  graver  blunder,  or  an  exhibition  of  profounder  ignorance 
in  the  domain  of  practical  geology. 

A  resolution  of  February  6,  1839,  adopted  by  the  house  of  repre- 
sentatives, reads  as  follows:  "  That  the  President  of  the  United  States 
be  requested  to  be  caused  to  be  prepared,  and  presented  to  the  next 
congress,  at  an  early  day,  a  plan  for  the  sale  of  the  public  mineral 
lands,  having  reference  as  well  to  the  amount  of  revenue  to  be  derived 
from  them,  and  their  value  as  public  property,  as  to  the  equitable 
claims  of  individuals  upon  them ;  and  that  he,  at  the  same  time,  com- 
municate to  congress  all  the  information  in  possession  of  the  treasury 
department  relative  to  their  location,  value,  productiveness,  and  occu- 
pancy; and  that  he  cause  such  further  information  to  be  collected, 
and  surveys  to  be  made,  as  may  be  necessary  for  these  purposes."  In 
pursuance  of  this  resolution,  the  commissioner  of  the  general  land 
office  appointed  Dr.  D.  D.  Owen  to  take  charge  of  a  geological  survey 
of  the  Upper  Mississippi  lead  region.  Dr.  Owen  began  his  work, 
with  139  assistants,  in  September,  1839,  and  finished  it  the  same 
autumn.  His  report,  accompanied  by  maps,  drawings  of  fossils,  sec- 
tions, etc.,  was  transmitted  to  the  land  office,  April  2,  1840.  It  was 
printed  without  the  maps  in  June  of  the  same  year. 

The  senate  ordered  it  reprinted,  with  the  maps  and  drawings,  in 
1844.  Dr.  Owen's  report  contains  the  first  scientific  description  of 
the  lead  region  of  Wisconsin.  With  a  few  mistakes,  easily  made  in 
a  hasty  survey,  without  skilled  assistants,  the  report  determines  the 
geological  structure  of  the  southwestern  part  of  the  state. 

The  general  government  authorized  a  geological  survey  of  the  Chip- 
pewa  land  district  in  1847,  and  Dr.  Owen  was  very  fortunately  selected 
to  take  charge  of  it.  His  preliminary  report  was  furnished  to  the 
treasury  department  in  April,  1848.  His  final  report  was  published, 
with  a  general  geological  map,  including  the  whole  state  of  Wisconsin, 
in  1851.  It  is  a  monument  of  Dr.  Owen's  industry  and  scientific 
knowledge.  Professor  J.  D.  Whitney,  a  most  competent  witness,  truly 
says,  speaking  of  his  previous  report,  "  There  were  probably  few,  if 
any,  persons  in  the  country,  at  that  early  period  of  our  geological  cul- 
ture, who  could  have  executed  the  survey  with  the  ability  and  energy 
which  were  displayed  by  this  gentleman." 

The  legislature  of  Wisconsin  passed  an  act,  approved  March  25, 

1853,  under  which  Mr.  Daniels  was  appointed  State  Geologist.     His 
report,  about  fifty  pages  in  length,  bears  no  date,  but  was  printed  in 

1854.  It  repeats  the  views  of  Dr.  Owen  and  is  mostly  confined  to  the 
lead  region.    About  a  year  afterwards,  Mr.  Daniels  was  removed,  and 


ANNUAL  REPORT  FOR  1875.  69 

Dr.  J.  Gr.  Percival  was  appointed  in  his  place,  August  12,  185-i.  He 
held  the  office  till  his  death  at  Hazel  Green,  May  2, 1856.  Dr.  Perci- 
val was  in  the  field  two  seasons.  His  first  report,  of  100  pages,  was 
published  under  his  own  supervision.  He  left  a  second  report  nearly 
complete,  which  was  subsequently  published  in  1856.  His  work  was 
mostly  confined  to  the  lead  region,  but  the  second  season  he  made  a 
"  reconnoissance  of  the  state  for  the  purpose  of  forming  a  general  idea 
of  the  geological  arrangement."  At  once  scientist  and  poet,  morbid 
and  eccentric,  Dr.  Percival  made  accurate  original  geological  observa- 
tions, but  refused  to  hold  intercourse  with  others  from  whom  he  might 
have  received  important  information  and  valuable  aid. 

In  March,  1857,  the  Wisconsin  legislature  passed  an  act  providing, 
that  "  James  Hall,  of  Albany,  K.  Y.,  and  Ezra  S.  Carr,  and  Edward 
Daniels,  of  Wisconsin,  are  hereby  designated  and  appointed  commis- 
sioners to  make  a  geological,  mineralogical,  and  agricultural  survey  of 
this  state,  embracing  a  scientific  and  descriptive  survey  of  the  rocks, 
fossils  and  minerals  of  the  state ;  full  and  complete  assays  of  the  ores 
and  minerals,  also  of  the  soils  and  subsoils,  with  classification  and 
description  of  the  same  and  their  adaptation  to  particular  crops,  and 
the  best  methods  of  preserving  and  increasing  their  fertility.  They 
shall  also  make  a  full  collection  of  the  rocks,  ores  and  minerals,  and 
whatever  illustrates  the  economic  geology  of  the  state,  and  deposit  the 
same  in  the  rooms  of  the  State  University,  or  such  other  place  as  may 
be  provided  for  the  same,  constituting  a  museum  of  practical  and  sci- 
entific geology.  Said  commissioners  shall  also  make  full  collections 
of  soils,  native  fertilizers,  cultivated  and  other  useful  plants,  constitut- 
ing a  museum  of  practical  and  scientific  geology,  and  deposit  the  same 
as  aforesaid."  The  act  also  provided  that  "  the  sum  of  six  thousand 
dollars  per  annum,  for  the  term  of  six  years,  is  hereby  appropriated, 
to  be  drawn  from  the  treasury  quarterly  on  warrant  of  the  governor, 
and  paid  to  persons  entitled  to  receive  the  same;  which  sum  shall  be 
in  full  for  salaries  of  commissioners,  assistants,  rent  of  room,  and  all 
other  expenses  incident  to  said  survey,  exclusive  of  printing  the  an- 
nual reports  of  said  commissioners." 

The  survey  thus  authorized  was  not  begun  until  the  following  year, 
1858.  In  that  year  Prof.  Hall  and  Dr.  Carr  employed,  at  their  own 
expense,  Col.  Charles  Whittlesey,  to  explore  the  country  between  the 
Menomonee  and  Oconto  rivers,  "  as  a  preliminary  to  more  extended 
surveys  to  the  northward."  In  the  spring  of  1859,  they  made  an  en- 
gagement with  Prof.  Whitney  to  make  a  careful  survey  of  the  lead 
region.  Prof.  Whitney  having  been  employed  as  chemist  and  miner- 
alogist in  the  Iowa  survey,  had  become,  to  a  certain  extent,  familiar 


70  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

with  the  upper  Mississippi  lead  region.  The  "Wisconsin  legislature 
passed  an  act,  approved  by  Gov.  Randall,  April  2,  1860,  author- 
izing the  governor  to  use  that  portion  of  the  fund  accruing  under  the 
law  of  1857,  from  the  signing  of  the  act  until  the  organization  of  the 
survey  in  1858,  to  the  payment  of  Prof.  Whitney  and  Col.  Whittlesey, 
and  also  making  Prof.  Hall  principal  of  the  geological  commission. 
Col.  Whittlesey  explored  the  country,  and  commenced  a  report  on  the 
iron  region  of  Lake  Superior.  Prof.  Whitney  completed  his  surveys, 
maps  and  reports  of  the  lead  region.  An  act  was  passed,  approved 
April  35,  1861,  authorizing  and  directing  the  governor  of  the  state 
"  to  purchase  of  Prof.  James  Hall  one  thousand  copies  of  the  first  vol- 
ume of  his  Geological  Report  of  Wisconsin,  confined  mainly  to  the 
lead  region,  with  the  details  of  the  geology,  mineralogy,  and  mining 
thereof;  and  to  contain  between  four  and  five  hundred  pages.  The 
said  volume  shall  embrace  a  chapter  on  the  general  geology  of  the 
state,  and  its  relation  to  the  surrounding  states,  and  shall  be  the  same 
size,  and  in  all  respects  as  to  type,  paper  and  binding,  equal  to  the 
Iowa  Geological  Report,  with  all  inecessary  maps  and  illustrations; 
provided,  that  the  said  one  thousand  copies,  delivered  at  the  capitol  in 
the  city  of  Madison,  shall  not  cost  more  than  three  dollars  each."  In 
1862,  the  said  first  volume  of  Prof.  Hall's  report  was  published  in 
accordance  with  the  specifications  of  the  law.  Prof.  Whitney's  re- 
port of  the  lead  region  occupies  three-fourths  of  the  volume.  Both 
Hall  and  Whitney  are  masters  in  this  field  of  science,  and  the  work 
of  both  was  well  done. 

The  next  year  the  legislature,  under  the  pressure  and  excitement  of 
the  war,  repealed  the  law  authorizing  the  geological  survey  of  the 
state.  Whereupon,  Dr.  Carr  and  Mr.  Daniels  abandoned  the  field. 
Not  so  Prof.  Hall.  He  had  a  contract,  under  seal,  with  the  governor, 
according  to  the  provisions  of  the  law,  and  claimed  that  the  legisla- 
ture could  not  annul  it.  He  continued  his  labor,  and  completed  that 
portion  of  his  work  which  had  been  assigned  to  him  in  its  division 
among  the  three  commissioners.  The  second  volume  of  his  report 
has  been  ready  for  publication  more  than  a  dozen  years.  Prof.  Hall 
has  made  repeated  applications  to  the  legislature  of  Wisconsin  for 
compensation,  but  in  vain.  We  are  informed  that  he  has  brought 
suit  against  the  state,  through  ex-Chief  Justice  Dixon,  for  two  thou- 
sand dollars  (a  year's  salary,  under  his  contract),  with  accrued  inter- 
est amounting  to  as  much  more.  The  second  volume  of  his  report, 
in  manuscript,  has  in  the  intervening  time  been  a  loss  to  science  and 
a  loss  to  the  economic  geology  of  Wisconsin.  It  contains,  we  are  in- 


ANNUAL  REPORT  FOR  1875.  71 

formed,  the  report  of  Col.  Whittlesey  on  the  iron  region  in  the  north- 
ern part  of  the  state. 

"  Descriptions  of  new  species  of  fossils,"  made  by  Prof.  Hall,  ac- 
companying his  report  of  progress  to  Gov.  Randall,  in  December, 
1860,  were  subsequently  embodied  in  the  first  volume  of  his  report, 
published  in  1862. 

The  report  of  John  Murrish,  as  commissioner  of  the  surrey  of  the 
lead  district,  made  to  Gov.  Lucius  Fairchild,  and  submitted  with 
the  governor's  message  in  1871,  contains  many  useful,  practical  sug- 
gestions by  an  experienced  miner  and  intelligent  man.  Whilst  this 
report  does  not,  in  our  judgment,  successfully  combat  the  scientific 
conclusions  of  Prof.  "Whitney,  it  exhibits  comprehensive  views,  and 
gives  valuable  hints  to  explorers  for  mineral  deposits.  Doubtless,  if 
the  labors  of  experienced  miners,  like  Mr.  Murrish,  and  the  labors  of 
purely  scientific  geologists  could  be  combined,  better  practical  results 
might  be  obtained. 

Under  the  provisions  of  the  present  law,  the  geological  corps  was 
organized  by  the  appointment  of  I.  A.  Lapham  as  chief  geologist, 
and  Prof.  R.  D.  Irving,  Prof.  T.  C.  Chamberlin  and  Mr.  Moses 
Strong  as  assistants.  The  commission  of  the  first,  issued  by  Gov.  C. 
C.  Washburn,  was  dated  April  10,  1873.  The  commissions  of  the 
assistants  were  dated  April  30,  1873. 

For  an  account  of  work  accomplished  by  this  corps  during  the  years 
1873  and  1874,  the  undersigned  has  the  honor  to  refer  your  excel- 
lency to  the  brief  reports  of  progress  made  by  the  chief  at  the  close 
of  those  years,  and  the  accompanying  voluminous  reports  made  by 
his  assistants,  together  with  maps,  profiles,  tables,  etc. 

The  commission  of  the  undersigned  bears  date  February  16,  1875. 
His  predecessor  was  appointed  by  Gov.  Washburn,  in  the  spring  of 
1873,  after  the  adjournment  of  the  legislature.  His  name  was  not 
sent  to  the  senate  for  confirmation  during  the  session  of  the  subse- 
quent legislature.  It  was  therefore  decided  (so  the  undersigned  is 
informed)  by  the  judiciary  committee  of  the  senate,  in  the  early  part 
of  the  session  of  the  last  legislature,  that  the  office  of  chief  geologist 
was  vacant.  His  Excellency,  Gov.  Win.  R.  Taylor,  did  the  under- 
signed the  honor  to  send  in  his  name  to  the  senate,  and  the  senate 

O  * 

confirmed  the  appointment  with  singular  "unanimity. 

The  assistant  geologists,  following  a  rule  of  courtesy  under  such  cir- 
cumstances, offered  to  surrender  their  commissions.  The  newly  ap- 
pointed chief  requested  them  to  withdraw  their  resignations,  and  to 
continue  their  work.  With  this  request  they  cheerfully  complied. 


72  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

The  resignation  of  Prof.  Daniells.  however,  as  chemist  to  the  survey, 
was  accepted  after  due  deliberation,  and  the  undersigned  appointed  in 
his  place  Mr.  Gustavus  Bode,  of  Milwaukee,  whose  acknowledged 
eminence  in  his  scientific  speciality  was  a  guaranty  of  peculiar  fitness 
for  the  work  entrusted  to  his  care  and  skill. 

Mr.  E.  T.  Sweet,  who  had  been  connected  with  the  survey  from  the 
beginning,  a  trained  geological  observer,  an  experienced  practical 
chemist,  was  employed  in  a  general  way,  to  be  transferred  from  one 
field  party  to  another,  or  to  be  detailed  to  the  laboratory  of  the  State 
University  for  special  analytical  work. 

Mr.  Sweet  has  shown  himself  very  efficient  in  connection  with  Prof. 
Irving's  party,  in  connection  with  the  party  of  the  chief  geologist  in 
making  an  extensive  reconnoissance  of  the  northern  portion  of  the 
state,  and  in  the  labor  of  the  laboratory. 

Mr.  Charles  E.  Wright,  of  Marquette,  L.  S.,  Michigan,  a  partner 
as  mining  engineer  and  iron  expert  of  Maj.  T.  B.  Brooks,  with  whom 
he  was  engaged  on  the  geological  survey  of  the  upper  peninsula  of 
Michigan,  was  employed  during  two  months  in  making  explorations 
at  Penokee  Gap,  on  the  Chippewa,  Wisconsin,  Pelican  and  Wolf 
rivers,  under  the  personal  supervision  of  the  undersigned.  His  ex- 
perience among  crystalline  rocks,  his  knowledge  of  the  Laurentian 
and  Huronian  formations,  and  his  skill  in  detecting  under  the  micro- 
scope the  difference  between  crystallization  by  igneous  action  and  met- 
amorphosis, made  his  services  of  especial  value  in  a  reconnoissance  of 
the  Archaean  region  of  Wisconsin. 

RECONNOISSANCE  MADE  IN  THE  NORTHERN  PART  OF  THE  STATE  UNDER 
THE  PERSONAL  DIRECTION  OF  THE  CHIEF  GEOLOGIST,  DURING  THE  LAT- 
TER PORTION  OF  THE  SEASON  OF  1875.  —  About  the  middle  of  August 
the  state  geologist  began  an  extensive  reconnoissance  of  the  northern 
portion  of  Wisconsin,  for  the  general  purpose  of  ascertaining  the  na- 
ture and  amount  of  work  to  be  done  to  complete  the  survey  in  1876. 
The  reports  of  the  surveys  made  by  Dr.  Owen  and  by  Messrs.  Foster 
and  Whitney,  were  carefully  studied  and  extensive  notes  taken,  for 
the  purpose  of  having  a  sort  of  geological  guide  book  of  the  region, 
and  for  the  purpose  of  avoiding  an  unnecessary  repetition  of  work 
already  performed  and  recorded.  Maps,  camping  materials,  supplies, 
instruments,  etc.,  were  collected  beforehand,  and  all  preparations 
made  for  moving  as  rapidly  as  possible,  and  covering  the  greatest 
amount  of  territory  in  a  given  time. 

Mr.  E.  T.  Sweet,  a  seasoned  explorer,  a  good  geological  observer,  a 
hardy  and  enthusiastic  worker,  who  had  had  experience  in  the  north- 


ANNUAL  REPORT  FOR  1875.  73 

ern  wilderness  of  Wisconsin,  was  detailed  from  the  field  party  of  Prof. 
Irving,  to  accompany  the  chief  geologist  during  the  whole  trip. 

Charles  E.  Wright,  E.  M.,  of  Marqnette,  Michigan,  a  highly  edu- 
cated lithologist  and  mining  engineer,  who  had  had  many  years  of 
experience  among  the  crystalline  rocks  of  the  upper  peninsula  of  Mich- 
igan, was  engaged  to  meet  the  party  at  Ashland  on  the  first  of  Sep- 
tember, and  to  continue  with  it  till  the  close  of  the  reconnoissance. 

For  the  details  of  the  work  accomplished,  your  excellency  is  refer- 
red to  the  reports,  maps  and  sections  of  Mr.  Sweet  and  Mr.  Wright, 
which  are  herewith  submitted. 

Among  the  objects  designated  in  advance  to  be  accomplished  by 
the  reconnoisance,  were  to  observe  the  trap  dykes  (the  Copper-bearing 
rocks  of  Mr.  Sweet's  report)  crossing  the  St.  Croix  river,  and  to  ascer- 
tain their  direction ;  to  study  the  relation  of  these  same  dykes  to  the 
Potsdam  sandstone  and  to  the  Lake  Superior  red  sandstone";  to  collect 
facts  bearing  upon  the  relative  age  of  the  Potsdam  sandstone  and  the 
Lake  Superior  sandstone;  to  investigate  the  relations  of  the  copper- 
bearing  conglomerate  to  the  older  and  the  more  recent  formations;  to 
make  a  more  careful  and  accurate  geological  section  of  Penokee 
mountain;  to  determine  the  general  direction  of  that  range,  and  the 
probable  locality  where  it  crosses  the  St.  Croix  river;  to  find,  by  long 
journeys  northward  and  southward  on  the  Chippewa,  Black,  Wiscon- 
sin and  Wolf  rivers,  boundary  points  between  the  Huronian  and  Lau- 
rentian  formations;  to  discover  indications  of  mineral  deposits;  and  to; 
collect  information  in  regard  to  roads,  bridle  paths,  trails,  and  streams 
navigable  for  canoes,  in  order  to  enable  the  chief  geologist  to  give  in- 
telligent directions  for  conducting  the  survey  in  detail  next  season, 
with  economy  and  efficiency. 

The  numerous  trap  dykes  crossing  the  St.  Croix  river  were  found 
to  run  in  a  general  east-northeast  and  west-southwest  direction,  nearly 
parallel  to  each  other. 

There  are  three  trap  ridges  between  Osceola  Mills  and  the  village 
of  St.  Croix  Falls;  whether  these  dykes,  so  called,  are  of  the  samo 
age,  is  a  problem  to  be  solved  by  future  examinations. 

Whether  they  are  igneous  in  origin,  or  whether  a  portion  of  them 
are  of  igneous  origin  and  another  portion  are  not,  can  only  be  deter- 
mined by  a  more  careful  examination  of  their  crystalline  structure 
under  the  microscope.  The  Canadian  geologists  have  made  out,  on 
the  northern  shore  of  Lake  Superior,  several  systems  of  trap  dykes, 
evidently  of  different  eruptive  periods;  but  the  geological  character 
of  the  region  on  the  southern  shore  of  the  lake  is  so  different  in  many 
respects  from  that  of  the  opposite  shore,  that  no  trustworthy  argument 


74  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

can  "be  drawn  from  analogy.  It  is  sufficient  to  remark  here  provision- 
ally, that  the  apparent  common  lithological  character  and  the  same 
general  trend  of  the  trap  ridges  crossing  the  St.  Croix  river  would 
point  to  the  same  geological  era. 

A  somewhat  careful  examination  at  St.  Croix  Falls  enabled  the  ex- 
ploring party  to  determine  that  the  Potsdam  sandstone  was  deposited 
in  the  ancient  Silurian  sea  at  a  period  subsequent  to  the  formation  of 
the  trap,  whatever  may  have  been  its  origin.  The  beds  of  the  Pots- 
dam sandstone  are  horizontal  over  the  uneven  and  tilted  surface  of 
the  underlying  igneous  or  crystalline  rocks. 

Almost  in  contact  with  the  trap,  the  sandstone  contains  numerous 
well  preserved  organic  remains.  Three  miles  north  of  Osceola  Mills, 
a  ledge  of  sandstone  was  found  lying  horizontal,  unconformably  on 
the  more  ancient  formation.  These  facts  incontestably  prove,  that 
this  particular  trap  dyke  was  not  erupted  or  upheaved  through  a 
superincumbent  layer  of  sandstone. 

At  Kettle  river  rapids  was  first  found,  in  ascending  the  river,  a  red 
sandstone,  having  all  the  lithological  characteristics  of  the  Lake  Su- 
perior red  sandstone,  in  talus  along  the  shore.  The  water  in  the  river 
was  extremely  low,  so  that  unusual  opportunity  was  afforded  for  ob- 
servation. The  slabs  and  fragments  of  the  red  sandstone  were  sharply 
angular,  showing  that  they  were  in  situ  or  not  far  away.  In  the 
bank,  forty  or  fifty  feet  higher,  was  a  fine  exposure  of  Potsdam  sand- 
stone in  a  massive  ledge. 

The  party  had  neither  the  time  nor  the  means  at  its  disposal  to 
make  an  excavation  to  ascertain  by  definite  observation  whether  the 
Superior  red  sandstone  existed  in  true  formation  beneath  the  Potsdam. 
Such  a  fact,  definitely  settled  by  a  competent  observer,  would  be 
strong  evidence  that  the  former  is,  at  least  in  part,  older  than  the 
latter. 

At  "  Pine  Island,"  in  the  same  rapids,  the  Superior  red  sandstone 
was  found  in  ledge,  bearing  abundant  angular  fragments  of  the  adja- 
cent trap,  forming  a  brecciated  conglomerate  that  is  evidently  kindred 
to  the  conglomerate  that  extends  from  Keweenaw  Point,  in  Michi- 
gan, along  the  northern  base  of  the  Porcupine  and  Penokee  mountains, 
west  southwestward,  till  it  is  lost  beneath  the  heavy  drift  of  north- 
M'estern  Wisconsin.  Everywhere  this  conglomerate  is  formed  by 
fragments  of  the  more  elevated  Huronian  or  trap  ridges,  carried  down 
by  the  action  of  the  elements  and  imbedded  in  the  Superior  red  sand- 
stone. The  ledge  of  conglomerate  under  consideration  was  found  to 
be  lower  than  the  horizon  of  the  neighboring  Potsdam.  Placing  the 
conglomerate  and  the  Superior  red  sandstone  in  the  same  geological 


ANNUAL  REPORT  FOR  1875.  75 

category,  tliis  fact  goes  far  to  strengthen,  if  not  confirm,  the  conject- 
ure, advanced  in  the  preceding  paragraph. 

Another  fact  has  considerable  bearing  upon  the  same  point.  The 
Superior  red  sandstone,  wherever  it  borders  on  the  trap  ridges,  shows 
that  it  has  been  tilted,  broken  up  or  crushed.  It  therefore  appears, 
that  the  trap,  whether  erupted,  or  upheaved  convulsively  or  slowly, 
encountered  this  formation,  in  its  ascent.  On  the  contrary,  as  we 
have  already  seen,  the  Potsdam  exhibits  undisturbed  horizontal  bed- 
ding on  the  trap.  One  of  two  things  necessarily  follows:  either  the 
Superior  red  sandstone  is  older  than  the  Potsdam,  or  the  trap  rocks, 
wherever  they  occur  in  conjunction  with  the  Superior  red  sandstone, 
are  younger  than  where  they  occur  in  conjunction  with  the  Potsdam. 
The  evidence  is  not  conclusive,  but  it  is  strongly  corroborative. 

Again,  it  is  known  that  the  Superior  red  sandstone  has  a  much 
greater  thickness  than  the  Potsdam.  In  the  region  of  Montreal  river, 
its  thickness  has  been  computed  at  five  thousand  feet.  By  trigono- 
metrical calculation,  Mr.  Sweet  has  found  its  thickness  to  be  about 
four  thousand  feet  on  the  upper  St.  Croix.  The  Potsdam  in  Wiscon- 
sin is  not  over  nine  hundred  feet  thick. 

Now  it  is  evident  that  the  Superior  red  sandstone  must  have  been 
much  longer  in  forming  than  the  Potsdam.  As  the  former  does  not  be- 
long to  a  later  period,  a  portion  of  it  must  certainly  antedate  the  latter. 

Awaiting  then,  a  longer  and  more  careful  study  and  more  extensive 
and  accurate  collection  of  facts,  it  may  be  conjectured  that  the  lower 
and  thicker  portion  of  the  Superior  red  sandstone  is  synchronous  with 
and  the  equivalent  of  the  Acadian  epoch  of  Dawson,  in  the  Canadian 
survey,  while  the  upper  and  thinner  portion  is  synchronous  with,  and 
the  equivalent  of  the  Potsdam  sandstone  of  the  New  York  geologists, 
which  is  represented  over  a  wide  area  of  Wisconsin.  The  argument 
from  paleontology  has  no  bearing  on  this  difficult  question.  The  red 
sandstone  of  the  Lake  Superior  region  is  without  organic  remains. 
The  Potsdam  of  Wisconsin,  while  it  is  rich  in  fossils,  contains  no 
species  that  is  identical  with  any  species  in  the  Potsdam  of  New 
York.  The  epoch  of  the  formation  is  determined  solely  on  strati - 
graphical  grounds,  by  its  relation  to  the  underlying  Archaean,  and  to 
the  overlying  Calciferous  of  the  Canadian  group,  or  the  Lower  Mague- 
sian  limestone. 

The  journey  from  the  head  of  St.  Croix  river  to  Bayfield  confirmed 
previous  information,  that  the  country  is  covered  with  drift  to  such 
an  extent  as  to  make  satisfactory  geological  exploration  an  impossi- 
bility. There  is  not  an  outcrop  of  rocks  for  fifty  miles.  Most  of  the 
region  is  destitute  of  living  springs  and  streams.  Numerous  depres- 


76  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

sions  in  the  drift  are  partly  filled  with  water,  forming  lakelets  without 
inlet  or  outlet.  Some  of  these  little  lakes  are  large  enough  to  be  kept 
pure  by  the  action  of  the  winds  and  waves.  The  soil  is  sandy  and 
barren,  supporting  only  a  stinted  growth  of  "jack"  pines  and  "  scrub 
oaks."  Fire  has  killed  the  timber  over  wide  areas,  on  which  grass 
was  growing,  exhibiting  before  our  eyes  nature's  simple  method  of 
converting  woodland  into  prairie.  The  reverse  process  is  just  as 
simple.  When  prairies  are  no  longer  swept  over  by  fire,  timber 
springs  up,  reconverting  prairie  into  woodland.  Grass,  with  fire  as 
an  ally,  can  beat  timber.  Timber  can  beat  grass  when  it  has  no  fire 
to  fight. 

The  same  kind  of  "Jack"  pine  barrens,  interspersed  with  prairie, 
extends  from  a  short  distance  above  St.  Croix  Falls  to  the  basin  of  Lake 
Superior.  Along  the  streams,  on  the  "bottom"  lands,  there  is  a 
heavy  growth  of  timber,  including  white  pine,  oak,  poplar,  and  maple. 
Towards  the  sources  .of  the  streams  flowing  into  the  St.  Croix  from 
the  Wisconsin  side,  are  many  fine  forests,  supplying  vast  quantities 
of  lumber.  In  the  basin  of  Lake  Superior,  the  soil  is  fertile,  support- 
ing great  forests  of  Norway  pine,  some  white  pine,  hemlock,  maple, 
etc.  The  agricultural  capabilities  of  the  St.  Croix  valley  are  not  very 
great.  The  farmer  could  look  to  the  basin  of  Lake  Superior  much 
more  hopefully  for  a  reward  of  industry  and  enterprise. 

A  new  geological  "  section  "  of  the  Penokee  range  was  made  by  the 
party  at  Penokee  Gap,  along  Bad  river,  where  the  Wisconsin  Central 
railroad  crosses.  For  a  clear  description  of  the  structure  of  this  Hu- 
ronian  formation,  your  excellency  is  referred  to  the  special  report  of 
Charles  E.  Wright  and  the  accompanying  chart. 

In  the  most  conclusive  manner,  the  unconformabitity  of  the  overly- 
ing northward  dipping  Huronian,  to  the  underlying  southward  dipping 
Laurentian,  is  made  out. 

The  undersigned  is  less  reserved  than  Mr.  Wright  in  expressing  an 
opinion  as  to  the  value  of  the  iron  deposit  in  the  Penokee  range. 
Careful  chemical  analyses  of  good  specimens  of  magnetic  ore  show 
that  it  is  very  rich  in  metallic  iron,  that  it  is  free  from  titanic  acid, 
that  it  contains  very  little  phosphorus,  that  silica  is  not  sufficiently 
abundant  to  seriously  interfere  with  its  reduction  in  the  furnace. 

Well  selected  specimens  have  shown  from  sixty  to  sixty-eight  per 
cent,  of  iron,  of  fine  quality.  To  scientists  it  is  not  necessary  to  state 
that  the  richest  possible  iron  ore  is  a  pure  magnetite  which  yields 
seventy-two  and  forty-one  hundredths  per  cent,  of  metal.  It  is  sim- 
ply a  popular  delusion  that  there  are  ores  rich  enough  to  yield  sev- 
enty-five, eighty  or  eighty-five  per  cent,  of  iron . 


ANNUAL  REPORT  FOR  1875.  7f 

It  is  an  important  fact,  that  Mr.  Wright  found,  by  microscopic  ex- 
amination, the  crystalline  structure  of  the  Penokee  rocks,  to  be  meta- 
morphic  and  not  igneous.  His  authority  on  this  point  is  conclusive. 

Whether  the  Huronian  formation  of  the  Penokee  mountain  extends 
westward  to  the  St.  Croix  river,  is  a  question  of  great  interest,  both 
in  the  scientific  and  economic  geology  of  Wisconsin.  Awaiting  de- 
ductions from  more  detailed  examination  to  be  made  by  the  survey  in 
1876,  the  undersigned  may  here  give  the  arguments  in  favor  of  such 
a  conclusion,  taken  from  the  report  of  Mr.  Sweet,  who  has  had  more 
experience  in  this  part  of  the  state  than  any  other  member  of  the 
geological  corps: 

"  I.  The  westward  extension,  and  occurrence  on  the  St.  Croix  river, 
of  all  the  formations  in  their  regular  order,  except  the  horizontal  sand- 
stone formed  north  of  the  Penokee  range,  is  a  strong  argument  from 
analogy.  We  can  not  expect  to  find  as  well  defined  ridges  nor  as 
high  ranges  near  the  St.  Croix  as  there  are  in  the  eastern  part  of  Ash- 
land county,  for  the  dip  of  all  the  formations  gradually  decreases  to- 
wards the  west.  The  dip  of  the  Huronian  schists  at  the  gorge  at 
Tyler's  Fork  is  75°  to  the  northwest.  At  Penokee  Gap  it  is  66°,  and 
at  a  point  near  Atkins  Lake  only  45°  in  the  same  direction.  The 
conglomerates  and  sandstones,  which  have  nearly  a  vertical  dip  to  the 
northwest  at  the  mouth  of  the  Montreal  river,  and  the  mouth  of 
Tyler's  Fork,  have  but  a  slight  dip  on  the  St.  Croix  river.  At  Lc- 
high's  on  Bad  river,  the  southward  dipping  sandstones  have  a  dip  of 
38°  to  the  southeast;  at  Wilton's  the  dip  is  26°;  at  the  St.  Croix  only 
14°  to  the  southeast. 

"  II.  If  the  Iron-bearing  belt  extends  westward  as  far  as  the  St. 
Croix,  it  doubtless  follows  the  southern  boundary  of  the  Cupriferous 
formation.  It  would,  therefore,  intersect  the  river  some  distance  below 
the  mouth  of  Snake  river.  Then  in  the  neighborhood  of  a  line  drawn 
from  Snake  river  to  Penokee  Gap,  one  would  expect  to  find  indica- 
tions of  the  formation." 

Iron  ore  is  reported,  by  explorers,  to  have  been  found  in  place,  at 
several  localities  in  the  vicinity  of  this  line. 

Explorers  report  it  from  near  the  southern  end  of  Long  Lake,  from 
section  18,  town  43,  range  9  west,  and  from  the  northern  part  of  Bur- 
nett county.  .Near  the  mouth  of  Wood  river,  on  section  19,  town  38, 
range  19  west,  are  found  on  the  original  survey  plat  the  signs  used  to 
indicate  rocks  in  situ,  and  the  words  "iron  ore." 

"  III.  The  occurrence  of  small  angular  boulders  of  magnetic  rock 
and  iron  ore,  in  the  drift  at  numerous  localities  in  Polk  and  Burnett 
counties,"  is  another  strong  argument. 


78  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

"  IY.  In  Michigan  and  in  all  regions  where  magnetic  iron  ore  is 
found,  much  reliance  in  exploring  is  placed  upon  magnetic  surveys. 
Valuable  mines  have  been  discovered  by  noting  the  abnormal  deflec- 
tions of  a  delicate  magnetic  needle  in  passing  along  at  right  angles 
to  the  trend  of  formations.  This  method  often  succeeds,  when  the 
dip  compass'  fails.  Although  magnetic  surveys  have  not  been  made 
in  the  region  under  consideration,  lineal  surveys  have,  and  the  varia- 
tion at  several  points  of  each  section  recorded  upon  the  township  plats. 

"  In  the  townships  through  which  the  Huronian  belt  would  be  ex- 
pected to  pass,  the  difference  between  the  maximum  and  minimum 
deflection  to  the  east  is  much  greater  than  in  townships  known  to  be 
distant  from  magnetic  influences. 

"  For  instance,  township  37,  range  20  west,  the  difference  is  5°  39', 
and  township  36,  range  20  west,  the  difference  is  5°  30'.  Numerous 
other  instances  might  be  mentioned.  The  fluctuations  of  the  needle 
from  a  fixed  point  under  ordinary  circumstances,  is  not  usually  over 
one  to  two  degrees." 

It  is  only  necessary  to  add  here  that  the  explorations  in  the  Peno- 
kee  range  for  the  discovery  of  iron  ore  would,  in  the  judgment  of 
the  undersigned,  be  more  likely  to  prove  successful,  if  they  were 
confined  to  boring  with  the  diamond  drill  into  the  northern  brow  of 
the  mountain  at  right  angles  to  the  dip  of  the  rocks  of  which  the 
formation  is  composed.  The  better  ores  are  softer;  therefore  have 
undergone  more  denudation  than  the  harder  ores ;  consequently  the 
former  are  buried  under  surface  debris,  whilst  the  latter  are  exhibited 
in  outcrop.  By  traversing  the  magnetic  schists  with  the  diamond  drill, 
the  quality  of  the  borings  can  be  constantly  tested,  and  the  true  hori- 
zon of  valuable  ores  can  be  accurately  ascertained. 

The  long  journeys  down  the  Chippewa  river,  from  the  crossing  of  the 
Central  railroad  to  Eau  Claire,  up  the  Wisconsin  river  from  Wausau 
to  the  mouth  of  the  Pelican,  up  the  Pelican  to  its  source,  and  down 
the  Wolf  from  a  short  distance  above  Post  Lake  to  Shawano,  were 
fertile  in  negative  results,  but  afforded  too  few  data  to  determine  with 
any  degree  of  accuracy,  boundaries  between  the  Huronian  and  the 
Laurentian  formations  in  the  wild  Archaean  region  of  the  state.  Ap- 
parently the  Chippewa  river  traverses  an  area  of  Laurentian  till  it 
touches  the  Potsdam  sandstone  in  its  southeastward  course.  A  Hu- 
ronian range  is  known  to  enter  the  state  from  the  Michigan  side,  at 
and  above  the  mouth  of  Pine  river  on  the  Menomonee,  and  to  extend 
westward.  At  Post  Lake  dam,  on  the  Wolf  river,  highly  crystalline 
hornblende  rocks  were  examined,  which,  with  other  indications,  led 
to  the  conjecture,  that  the  Menomonee  Huronian  range  crosses  in  that 


ANNUAL  REPORT  FOR  1875. 


79 


region.  Similar  indications  were  found  on  Pelican  river,  and  to  the 
northwest  of  Pelican  Lake. 

The  "  Greenstone  group  "  found  between  Jenny  and  Grandfather 
Bull  Falls  on  the  Wisconsin  river,  the  quartzite  near  "Wausau,  and 
the  silicious  rock  of  Marshall  hill,  evidently  Huronian,  give  additional 
points  for  determining  the  general  direction  of  the  Menomonee  range. 
The  southwestern  termination  of  it,  where  it  disappears  under  the 
Potsdam,  would  seem  to  be  at  Bladk  Hiver  Falls.  Between  this 
range  and  the  Penokee  mountain  range  there  is  probably  a  nearly  con- 
tinuous area  of  Laureiitian.  And  between  the  Menomonee  Huronian 
range  and  the  irregular  line  of  the  northern  edge  of  the  Potsdam 
there  is  a  continuous  Laurentian  belt. 

The  geographical  boundaries  of  these  formations  can  only  be  deter- 
mined by  more  detailed  explorations. 

It  is  a  matter  of  great  practical  importance  to  trace  the  outlines  of 
the  Huronian  and  Laurentian  formations  in  the  Archaean  region  of 
the  state,  for,  judging  from  results  obtained  from  the  adjacent  region 
of  the  Upper  Peninsula  of  Michigan  where  exactly  the  same  forma- 
tions exist,  the  Laurentian  rocks  contain  no  useful  minerals,  while 
the  Huronian  areas  promise  an  abundance  of  iron,  if  not  more  pre- 
cious metals. 

HAMILTON  on  LOWER  HELDERBEKG?  — There  is  a  region  of  "Wiscon- 
sin, on  the  shore  of  Lake  Michigan,  beginning  in  the  city  of  Milwau- 
kee, extending  northward  to  the  vicinity  of  the  county  line  of  Ozaukee, 
running  inland  half  a  dozen  miles,  shaped  something  like  a  segment 
of  a  circle,  which  has  been  placed  by  geologists  in  the  Upper  Helder- 
berg  epoch,  and  has  been  called  by  one  scientist  in  connection  with 
the  present  survey  of  the  state,  the  Hamilton  formation. 

The  undersigned,  soon  after  he  began  studying  the  geology  of  "Wis- 
consin, was  led  to  doubt  whether  the  region  in  question  belongs  to  the 
Devonian  age,  as  it  must,  if  it  is  either  Upper  Helderberg  or  Hamil- 
ton. The  proper  place  for  a  full  discussion  of  the  subject  will  be  in 
the  final  report,  after  the  geological  survey  of  the  state  is  completed. 
Yet  it  may  not  be  out  of  place  to  give  here,  briefly  as  may  be  consist- 
ent with  clearness,  the  reasons  which  have  forced  the  present  head  of 
the  survey  to  conclude,  against  his  predecessors,  against  his  associates, 
that  the  limited  area  under  consideration  is  Lower  Helderberg,  and 
consequently  belongs  to  the  Upper  Silurian  and  not  to  the  Devonian 
age. 

In  North  American  Geology,  following  the  nomenclature  of  Prof. 
Dana  and  the  New  York  geologists,  the  proper  place  of  the  Lower 


SO  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

Helderberg  is  above  the  Salina  and  below  the  Oriskany.  Of  course, 
its  stratigraphical  relations  vary  in  localities.  The  normal  underlying 
formations  will  be  wanting  where,  during  one  or  more  preceding 
epochs,  emergence  of  the  land  had  taken  place  and,  consequently,  the 
ancient  ocean,  having  receded,  was  not  there  busy  with  its  work  of 
rock-making. 

For  the  same  reason,  in  many  localities,  the  normally  overlying 
series  are  entirely  wanting.  The  Lower  Helderberg,  like  the  rocks  of 
any  other  period,  are  entirely  wanting,  where  the  dry  land  had  ap- 
peared before  that  particular  epoch.  Over  a  large  area  of  Wisconsin, 
for  example,  there  are  no  rocks  above  the  Archaean,  for  the  simple 
reason  that  this  area  has  been  an  emerged  portion  of  the  continent 
since  the  primeval  ocean  first  deposited  the  Lauren tian  and  Huronian 
formations.  Nowhere  in  the  state  do  we  find  rocks  of  the  Mamma- 
lian, Reptilian,  or  Carboniferous  ages,  because  during  all  these  long 
divisions  of  geological  time,  Wisconsin  has  been  dry  land.  In  other 
places  on  the  globe,  the  seas  have  continued  their  labor  of  rock-making, 
but  here  the  continent  was  finished  long  ago.  In  places  portions  of 
the  continent  have  been  upheaved  during  one  or  more  periods,  and 
then  for  a  season  submerged  again  by  faster  or  slower  subsidence. 
During  the  period  of  emergence,  rock-making  has  ceased;  with  re- 
submergence  rock-making  has  gone  on  again.  Thus  epochs  are  want- 
ing here  and  there,  and  the  geologist  has  dynamical  problems  to  solve 
more  difficult  than  problems  of  lithology. 

The  Lower  Helderberg  epoch  takes  its  name  from  the  Helderberg 
mountains  in  the  state  of  New  York,  where  the  formation  is  com- 
plete. Beginning  from  below,  its  subdivisions  are:  (1)  The  Tentacu- 
lite  or  Water-lime  group;  (2)  The  Pentamerus  limestone;  (3)  The 
Catskill  or  Delthyris  shaly  limestone;  (4)  The  Encrinal  limestone, 
and  (5)  The  Upper  Pentamerus  limestone. 

In  this  connection,  it  is  necessary  to  consider  more  particularly  the 
lowest,  or  Water-lime  division.  In  fact,  the  different  subdivisions  ob- 
served in  the  Helderberg  mountains,  scarcely  appear  outside  of  New 
York  state.  All  of  them  but  the  Water-lime  group  disappear,  even  in 
New  York,  westward  of  Ontario  county.  "  This  group,"  says  Mr. 
Yanuxem,  in  the  New  York  state  survey,  "  takes  its  name  from  its 
earthy  drab  colored  limestone,  from  which  all  the  water-lime  in  the 
district  south  of  the  Erie  canal,  with  one  exception,  is  manufactured. 
It  consists  generally  of  dark  blue  limestone,  and  usually  of  two  layers 
of  drab  or  water-lime  stone;  the  two  always  separated  by  an  inter- 
vening mass  of  blue.  The  group  is  well  defined,  and  is  readily  recog- 
nized in  this  state  and  in  Pennsylvania,  by  its  mineral  nature,  its  fos- 


ANNUAL  EEPORT  FOR  1876.  81 

sils  in  particular,  and  by  its  position."  Mr.  Yanuxem  traced  it  in 
that  early  date  to  Fort  Plain,  Cherry  Valley,  Richford  Springs,  vari- 
ous points  in  Oneida  county,  Onondaga  Valley,  Syracuse,  Auburn 
and  Cayuga  Bridge.  It  must  not  be  forgotten,  however,  as  Sir  Wm. 
E.  Logan  points  out  (Geology  of  Canada,  p.  363),  that  Mr.  Vanuxem 
confounded  this  group,  in  part,  with  the  upper  portions  of  the  under- 
lying gypsiferous  series,  which  it  closely  resembles  in  lithological 
character. 

The  Lower  Helderberg  formation  extends  over  a  wide  region  of 
North  America.  Becrafts  mountain  and  Mount  Rob,  near  the  city 
of  Hudson,  are  isolated  monuments  of  this  geological  epoch.  The 
formation  extends,  in  a  broken  way,  through  Connecticut,  Massachu- 
setts, New  Hampshire,  Maine,  New  Brunswick  and  Nova  Scotia. 
According  to  Sir  Win.  E.  Logan,  there  are  outliers  of  Lower  Helder- 
berg at  Point  Gaspe  and  near  Montreal,  at  St.  Helens  Island,  at  Round 
Island,  at  Isle  Bizard,  at  cuttings  for  the  Grand  Trunk  Railway,  be- 
tween Point  Claire  and  St.  Anne.  The  distinguished  chief  of  the 
Canadian  survey  justly  remarks  (Geology  of  Canada,  p.  358):  "From 
these  scattering  outlying  patches,  it  would  appear  that  a  considerable 
area  in  the  Champlain  and  St.  Lawrence  valleys  was  once  continuously 
covered  with  rocks  of  the  Lower  Helderberg  group;  while  from  the 
unconformable  relation  of  these  to  the  formations  on  which  they 
repose,  it  is  evident  that,  prior  to  the  Lower  Helderberg  period,  the 
older  fossiliferous  strata  had  suffered  a  great  amount  of  denudation." 

This  group  extends  along  the  Apalachian  mountains  southward, 
through  southeastern  New  York,  New  Jersey,  Pennsylvania,  Mary- 
land and  Virginia.  The  formation  is  thicker  on  the  Potomac  river 
than  on  the  Hudson.  It  thins  out  to  the  westward  in  the  southern  as 
well  as  in  the  northern  portion  of  the  range. 

The  Water-lime  division  of  the  Lower  Helderberg  enters  Canada 
opposite  to  Buffalo,  and  according  to  Sir  Wm.  E.  Logan,  "  can  be  traced 
pretty  continuously,  in  a  band  varying  from  twenty  to  forty-five  feet 
in  thickness." 

Although  this  language  was  used  in  the  Canadian  report  of  1863, 
yet  strangely  enough,  Mr.  Newberry,  in  the  recent  Ohio  report,  says 
that  the  Water-lime  group  "  had  not  been  recognized  beyond  the  limits 
of  New  York  previous  to  1869."  In  that  year  Mr.  Newberry  dis- 
covered the  Water-lime  subdivision  of  the  Lower  Helderberg  on  the 
islands  in  the  upper  end  of  Lake  Erie,  and  on  the  adjacent  shore. 
"Since  our  first  identification  of  the  Water-lime,"  he  says  (Geological 
Survey  of  Ohio,  p.  137),  "  we  have  traced  it  over  a  very  large  area 
within  this  state,  and  have  learned  to  recognize  it  almost  at  a  glance 
Wis.  STIR.  — 6 


82  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

by  its  prevailing  lithological  characters.  "We  have  also  obtained  its 
characteristic  fossils  from  hundreds  of  localities.  The  result  of  our 
investigation  has  been  to  show,  that  the  Water-lime,  judged  by  the 
area  it  occupies,  with  its  outcrops,  is,  in  Ohio,  the  most  important  of 
all  the  Silurian  strata.  It  underlies  a  broad  belt  of  country  on  either 
side  of  the  Cincinnati  axis,  from  the  lake  shore  to  Hardin  county. 
There  the  two  belts  coalesce,  and  the  Water-lime  stretches  entirely 
over  the  arch,  forming  the  surface  rock  for  nearly  a  hundred  miles 
east  and  west.  Further  south  the  margin  of  the  Water-lime  sweeps 
around  the  blue  limestone  area,  exterior  to  and  parallel  with  that  of 
the  Niagara. 

"  South  of  the  national  road,  and  east  of  the  anticlinal  axis,  the 
Water-lime  forms  a  constantly  narrowing  belt,  which  passes  through 
the  counties  of  Madison,  Fayette,  Highland  and  Adams,  to  the  Ohio. 
In  parts  of  Adams  and  Highland  it  forms  a  feather  edge  on  the  flanks 
of  the  Cincinnati  arch,  beyond  which  the  Huron  shales  rest  directly 
on  the  Niagara.  This  shows  that  the  sea  in  which  the  Water-lime  was 
deposited  reached  but  part  way  up  the  slope  of  the  old  Silurian 
island." 

The  same  formation  extends  westward  into  Indiana.  In  western 
Tennessee  it  has  been  recognized  in  Stewart,  Benton,  Decatur,  Hardin 
and  Henry  counties. 

Worthen,  in  the  Illinois  reports,  refers  to  the  Lower  Helderberg 
epoch  a  silicious  limestone  directly  overlying  the  Cincinnati,  with  no 
intervention  of  the  Niagara  limestone.  "  No  beds  of  undoubted 
Niagara  age,"  says  Mr.  Worthen  (Illinois  Reports,  vol.  I.,  p.  127), 
"  were  ever  deposited  in  southern  Illinois,  but  in  their  place  these 
silicious  limestones,  representing  in  part  the  age  of  the  Lower  Helder- 
berg limestones,  and,  in  part,  the  Oriskany  sandstone  of  the  New 
York  series,  were  deposited,  resting  directly  upon  the  Cincin- 
nati group  of  the  Lower  Silurian."  "Again,"  says  Mr.  Worthen, 
giving  an  account  of  the  geology  of  Union  county  (Illinois  Eeport, 
vol.  III.,  p.  36),  "  the  Lower  Helderberg  formation  is  similar  in  its  ap- 
pearance here  to  the  outcrops  of  it,  already  described  in  the  foregoing 
report  on  Alexander  county,  and  it  may  be  described  as  a  thinly  bed- 
ded, grayish  colored,  close-textured,  silicious  and  cherty  limestone, 
sometimes  argillaceous  and  shaly,  and  again  so  flinty  that  it  is  dif- 
ficult to  say  whether  the  flint  or  the  limestone  predominates."  The 
flinty  character  of  this  formation  at  certain  localities  in  New  York 
was  fully  described  by  Mr.  Yanuxem. 

Following  the  Lower  Helderberg  northwestward  from  Buffalo, 
through  Canada,  we  find  rocks  with  the  same  lithological  characters 


ANNUAL  REPORT  FOR  1875.  83 

at  the  junction  of  Lake  Huron  and  Lake  Michigan,  occupying  the 
entire  island  of  Bois  Blanc,  occupying  most  of  the  small  peninsula 
west  of  St.  Martin's  Bay,  and  skirting  the  Straits  of  Mackinac  along 
the  northern  shore  of  the  southern  peninsula  of  Michigan.  It  over- 
lies the  Salina  formation,  and,  consequently,  is  in  the  exact  strati- 
graphical  place  of  the  Lower  Helderberg.  Speaking  of  these  same 
rocks,  Dr.  Rominger  says  (Geological  Survey  of  Michigan,  vol.  I.,  p. 
28,  of  his  division  of  the  subject),  "  Taking  into  consideration  the 
stratigraphical  sequence,  surmounted  above  by  well  characterized 
Upper  Helderberg  strata,  underlaid  below  by  beds  of  perfect  litholog- 
ical  resemblance  to  the  Onondaga  salt  group,  we  may  safely  take  th  e 
intermediate  beds  as  contemporaneous  with  the  Lower  Helderberg 
groxup." 

Now  the  formation,  under  discussion  in  the  state  of  Wisconsin,  has, 
so  far  as  the  underlying  strata  are  concerned,  the  same  stratigraph- 
ical relations  as  the  Water-lime  subdivision  of  the  Lower  Helderberg  in 
New  York,  Canada,  the  Appalachian  region  (and  westward  to  the 
Mississippi  river),  and  on  the  islands  and  adjacent  shores  of  Mackinac 
straits.  The  Salina  or  Onondaga  salt  group  underlies  it  here  as  else- 
where.1 

As  an  exception  to  the  general  statement,  if  Mr.  Worthen  is  cor- 
rect, not  only  the  Salina,  but  other  formations  are  wanting  below  the 
Water-lime  in  southern  Illinois,  down  to  the  Cincinnati  limestone. 
But  in  this  limited  region  of  Wisconsin,  the  underlying  Salina  is 
present,  and  crops  out  all  around  the  Water-lime  in  a  narrow  circular 
rim.2  The  ancient  Silurian  sea  slowly  receded  from  the  Archaean 
peninsula  in  northern  central  Wisconsin,  with  its  outlying  islands 
and  reefs,  depositing  in  turn  the  Potsdam  sandstone,  the -Calciferous 
or  Lower  Magnesian  limestone,  the  St.  Peters  sandstone,  the  Trenton 
limestone,  the  Galena  limestone,  the  Clinton  and  Niagara  groups,  the 
Salina,  and,  finally,  at  the  last  point  of  emergence,  the  Water-lime  base 
of  the  Lower  Helderberg. 

There  is  a  stronger  argument  from  stratigraphy  than  that  of  the 
normal  relations  of  the  Salina  and  the  Water-lime. 

If  the  formation  in  question  is  Hamilton,  then  the  absence  of  the 
intermediate  strata  must  be  accounted  for,  and  reconciled  to  the  facts 
of  local,  as  well  as  North  American  geology.  Between  the  Salina 

1  Recent  investigation  has  shown  that  the  rocks  here  called  Salina  are  themselves 
probably  the  Lower  Helderberg.    T.  C.  C. 

2  On  the  maps  published  previous  to  the  more  careful  investigations  o.f  the  present 
survey,  the  formation  was  represented  as  here  stated,  but  upon  confessedly  imperfect 
evidence.    It  is  now  shown  that  this  mapping  was  unwarranted.    T.  C.  C. 


84  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

and  the  Hamilton,  there  are  the  epochs  of  the  Lower  Helderberg  and 
the  Oriskany  in  the  Upper  Silurian  age  and  the  Cauda-galli,  Schoharie, 
Corniferous,  and  Marcellus  epochs  in  the  Lower  Devonian  age. 

During  all  that  long  period,  therefore,  while  the  ancient  sea  was 
depositing,  under  different  conditions,  these  half  dozen  formations, 
the  little  semi-circular  patch  of  Wisconsin,  under  discussion,  must 
have  been  dry  land,  with  the  Salina  for  surface  rock,  and  then  must 
have  become  submerged  long  enough  for  the  deposition  of  the  De- 
vonian Hamilton,  again  to  be  emerged  at  the  close  of  that  epoch,  and 
remain  dry  land  to  the  present  hour.  And  this  submergence  must 
have  been  just  far  enough,  according  to  such  a  hypothesis,  to  leave  at 
every  point  on  its  margin  a  semi-circular  rim  of  Salina.  It  would  be 
impossible  to  harmonize  a  supposition  of  this  kind  with  the  known 
facts  of  rock-structure  of  surrounding  regions,  or  to  make  it  con- 
sistent with  the  recognized  laws  of  dynamical  geology.  It  is  much 
more  rational  to  suppose  that  the  land  was  slowly  rising;  that,  con- 
sequently, the  Silurian  sea  was  slowly  receding;  that  the  last  edge  to 
emerge  was  the  region  in  question;  that  during  its  own  epoch  the 
Salina  was  deposited;  that,  emergence  still  slowly  going  on,  the 
"Water-lime  of  the  Lower  Helderberg,  being  next  in  order  of  time, 
was  laid  down  over  a  narrower  area,  after  which  the  ocean  disappeared 
from  our  shores,  leaving  the  territory  where  Wisconsin  now  is,  hence- 
forth a  part  of  the  abiding  continent. 

The  paleontological  indications  for  determining  the  age  of  the  for- 
mation are  far  less  satisfactory  than  the  stratigraphical.  There  is  no 
doubt  that  these  rocks  are  of  the  same  epoch  as  those  mapped  by  Mr. 
Rominger  in  the  Michigan  survey  at  the  Straits  of  Mackinac  as 
Helderberg.  He  says  (p.  28,  Paleozoic  rocks),  speaking  of  the  pale- 
ontological evidence:  "Lcperditia  alta  and  Spirifer  modestus  are 
known  as  Lower  Helderberg  species.  On  such  a  meagre  representa- 
tion of  such  a  rich  fauna,  I  would  hesitate  to  base  conclusions  regard- 
ing the  age  of  the  formation."  Yet,  as  already  stated  above,  he 
concludes  from  stratigraphy  that  the  rocks  are  Lower  Helderberg. 
The  undersigned,  while  investigating  the  lithological  and  stratigraph- 
ical characters  and  relations  of  the  formation,  has  left  mainly  to 
others  an  examination  of  its  fossils.  Orthis  plicata,  Avicula  rugosa 
and  Tentaculites,  designated  by  Mr.  Vanuxem  as  characteristic  of  the 
Water-lime  group,  have  been  found  by  the  chief  geologist  at  Humbolt 
Falls.  Leperditia  alta,  a  still  more  important  characteristic  fossil, 
has  also  been  found. 

The  most  satisfactory  paleontological  evidence  of  this  formation  is 
JEurypterus  remipes,  which  has  not  been  discovered  in  the  region. 


ANNUAL  REPORT  FOR  1875.  85 

It  is  only  fair  to  state  that  Prof.  Cliamberlin,  of  the  survey,  has 
designated  from  this  region  Ichthyolites,  Strophodonta  demissa, 
Atnjpa  occidentalis^  Spiriferina  zigzag,  casts  of  dermal  tubercles  of 
fish,  and  other  organic  remains,  which  he  regards  as  characteristic  of 
the  Hamilton  epoch;  yet  he  marks  a  large  percentage  of  these  speci- 
mens as  questionable,  and  does  not  take  into  account  fossils  that  are 
clearly  of  the  Water-lime  period.  *  The  paleontological  question  can 
only  be  settled  by  a  more  careful  and  ample  collection  of  organic  re- 
mains than  has  hitherto  been  made,  which  shall  be  submitted  to  Mr. 
Billings,  Mr.  Meek,  or  some  other  great  authority  in  this  difficult 
branch  of  science,  who  can  judge  with  ample  knowledge  and  without 
prejudice. 

"While  acknowledging  that  paleontological  evidence  is  of  the  highest 
value,  and  is  of  itself  sufficient  to  settle  the  age  of  a  formation,  when 
unmistakable  and  clear,  yet  we  are  reminded  that  the  fauna  of  Paleo- 
zoic time  in  the  northwest  differs  greatly  from  the  fauna  of  the  same 
time  in  the  east.  For  example,  the  Potsdam  of  Wisconsin,  as  said 
above,  does  not  contain  a  single  species  identical  with  any  species 
found  in  the  same  formation  in  New  York.  It  is  necessary  to  rely 
on  the  stratigraphical  relations  for  determining  its  age. 

The  lithological  evidence,  which,  ordinarily,  is  of  the  least  value, 
and  is  often  of  no  value  at  all,  may,  in  this  case,  be  regarded  as  of 
considerable  importance.  Prof.  Dana's  brief  description  of  the  Water- 
lime  as  "a  drab  colored  or  bluish  impure  limestone,  in  thin  layers," 
is  everywhere  characteristic  of  this  formation.  Its  lithological  char- 
acter does  not  essentially  change  in  different  regions,  which  ordinarily 
makes  lithological  evidence  in  geological  questions  so  unreliable. 

The  undersigned,  coming  to  the  conclusion,  mainly  on  stratigraph- 

1  This  remark  was  probably  not  intended  to  convey  the  full  significance  which  its  lan- 
guage might  seem  to  imply,  but  as  it  has  been  retained,  it  becomes  necessary  to  state 
that  it  was  evidently  made  under  a  misapprehension  of  the  character  of  the  fossils  in 
question.  At  Dr.  Wight's  request,  I  furnished  him  with  a  box  of  fossils  collected  from 
the  formation,  but  as  they  had  not  then  received  systematic  investigation,  a  portion  of 
the  labels  were  prudentially  marked  with  an  interrogation  point  in  accordance  with  the 
habit  of  conscientious  investigators,  but  there  were  a  sufficient  number  not  so  marked 
to  demonstrate  the  Hamilton  age  of  the  deposit.  There  were  no  fossils  characteristic 
of  the  Water-lime  period  contained  in  my  collection,  and  it  is  safe  to  say  that  none  ex- 
ist in  the  formation.  The  entire  collection  of  the  survey,  which  is  ample  for  the  deter- 
mination of  the  age  of  the  rock,  has  been  submitted  to  Prof.  R.  P.  Whitfield,  a  most 
eminent  authority,  who  pronounces  the  fauna  distinctively  Hamilton,  and  fully  substan- 
tiates the  correctness  of  my  position.  See  page  397.  The  question  of  the  hydraulic 
properties  of  the  rock,  which  is  independent  of  its  age,  first  received  my  attention  about 
one  year  previous,  and  would  have  been  discussed  in  my  annual  report  for  that  year,  but 
for  the  delay  in  the  analysis  of  specimens  sent  to  the  chemist  of  the  survey  for  that  pur- 
pose, June  12,  1874.  T.  C.  C. 


86  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

ical  evidence,  that  the  formation  under  consideration  is  the  Water-lime 
group  of  the  Lower  Helderberg,  predicted  from  the  lithological  char- 
acters of  the  rock,  that  the  region  would  prove  rich  in  hydraulic 
cement.  He  did  not  then  know  that  any  discovery  of  the  valuable 
commercial  properties  of  the  rock  had  been  made.  An  analysis  of 
specimens  furnished  Prof.  Gustavus  Bode,  chemist  of  the  survey,  con- 
firmed the  conclusion  and  the  prediction.  The  state  of  "Wisconsin 
may  be  congratulated  in  a  discovery  that  will  add  greatly  to  her  re- 
sources, to  her  industry  and  to  her  commerce. 

In  the  meantime,  Mr.  D.  J.  Whittemore,  E.  C.,  chief  engineer  of 
the  Chicago,  Milwaukee  and  St.  Paul  Railway,  a  well  known  Wiscon- 
sin scientist,  had  made  a  long  series  of  careful  experiments  to  test  the 
commercial  value  of  the  cement  rock  found  in  the  Water-lime  forma- 
tion under  consideration.  He  has  demonstrated  that  it  produces  a 
cement  of  better  quality,  consequently  of  higher  value,  than  any 
cement  now  produced,  either  in  America  or  Europe,  except  the  Port- 
land., 

The  following  resume  of  the  results  of  his  experiments  has  been 
kindly  furnished  by  Mr.  Whitteinore  himself: 

MILWAUKEE,  December  23,  1875. 
DR.  0.  "W.  WIGHT,  State  Geologist  of  Wisconsin : 

MY  DEAK  SIR:  In  compliance  with  your  request,  I  herewith  make  a  condensed  state- 
ment of  the  principal  results  attained  in  my  experimental  inquiry  as  to  the  value  of 
hydraulic  cement,  made  from  the  recently  discovered  stone  deposit  in  the  vicinity  of 
Washington  street  bridge,  near  this  city. 

For  the  purpose  of  comparison,  I  selected  from  very  many  samples  of  commercial 
cements  those  that,  after  a  few  days1  trial,  gave  indications  of  good  quality;  therefore, 
you  will  bear  in  mind,  that  the  average  strength  of  the  commercial  cement  experimented 
upon  by  me,  is  considerably  above  the  general  average  of  the  cements  in  our  market. 
In  both  manipulation  and  testing,  I  availed  myself  of  every  experiment  that  I  could 
well  devise  to  secure  uniform  treatment  throughout  my  inquiry. 

I  converted  the  natural  Milwaukee  stone  into  a  cement  by  the  usual  method  of  calcina- 
tion and  grinding,  and  experimented  upon  the  product  from  single  stones  separately; 
also  upon  the  mixed  products  of  two  stones  selected  from  widely  separated  localities  of 
the  ledge,  each  submitted  to  varied  degrees  of  torrification  in  the  preparation,  and  all 
gave  very  similar  results.  This  determines  quite  conclusively  that  within  the  limits 
hereinafter  mentioned  the  deposit  has  a  uniform  character,  a  matter  of  much  import- 
ance in  determining  its  value. 

My  experimental  tests  were  directed  to  detennining  the  following  features,  viz. : 

1st.  To  ascertain  the  tensile  strength  in  pounds  per  square  inch  of  mortar,  composed 
of  equal  weights  of  cement  and  sand,  at  the  age  of  ninety  days,  the  last  eighty-nine  in 
water. 

2d.  To  ascertain  the  breaking  strength  of  mortars  of  cement  mixed  with  definite  por- 
tions of  sand,  moulded  into  bars  one  inch  square,  and  resting  on  supports  three  inches 
apart,  and  broken  by  application  of  weight  in  the  middle.  Age  of  mortars  one  hundred 
days,  the  last  ninety-nine  in  water. 

3d.    To  ascertain  the  crushing  strength  in  pounds  per  square  inch  of  mortars  of 


ANNUAL  REPORT  FOR  1875. 


87 


cement,  inked  with  definite  portions  of  sand,  at  the  age  of  ninety  days,  the  last  eighty- 
nine  in  water. 

4th.  To  ascertain  the  adhesive  strength,  in  pounds  per  square  inch  of  mortars  com- 
posed of  equal  parts  of  cement  and  sand,  to  common  brick,  at  the  expiration  of  seventy 
days. 

The  following  table  is  a  compilation  of  the  average  of  all  of  my  determinations,  and 
is  derived  from  over  fifteen  hundred  individual  tests : 


Tensile 
Strength. 

Breaking 
Strength. 

Crushing 
Strength. 

Adhesive 
Strength. 

nil 

5.2  31 

c~s 
o    5  L 

Itol 
by 
Weight. 

2  Cement 
and 
1  Sand. 

1  Cement 
and 
2  Sand. 

1  Cement 
and 
1  Sand. 

1  Cement 
and 
2  Sand. 

1  Cement 
and 
3  Sand. 

1  Cement 
arid 
1  Sand. 

Average  of  Milwau- 

200 
19-2 

134 

80 

69 
44 

2.365 

1,477 

1,451 
799 

1,107 

488 

73H 

45K* 

Average  of  Commer- 

The  strengths  of  the  commercial  cements  are  derived  from  the  average  of  many  testa 
of  the  number  of  brands  represented  below. 

For  tensile  strength,  14  brands  of  cement. 

For  breaking  strength,  6  brands  of  cement. 

For  crushing  strength,  11  brands  of  cement. 

For  adhesive  strength,  9  brands  of  cement. 

I  desire  to  state  that  the  average  results  attained  by  the  Milwaukee  product  exceeded 
the  maximum  attained  by  the  best  of  the  commercial  cements. 

I  have  now  under  examination  the  product  from  a  section  of  the  Milwaukee  ledge 
extending  from  the  surface  to  a  depth  of  thirteen  feet,  running  through  eleven  layers, 
and  its  strength  compares  very  favorably  with  the  former  determinations  of  the  Milwau- 
kee cement. 

The  rock  from  which  the  cement,  experimented  upon,  was  made,  was  selected  from 
the  banks  and  bed  of  Milwaukee  river,  between  the  west  line  of  the  east  half  of  north- 
west quarter  of  section  No.  5,  town  7  north,  range  No.  22  east,  and  the  east  and  west 
quarter  line  of  section  No.  4,  same  town  and  range. 

Yours  Truly,  D.  J.  WHITTEMORE,  C.  E. 

ARTESIAN  WELLS.  —  As  an  addition  to  accounts  of  artesian  wells 
given  in  previous  reports,  the  survey  is  indebted  to  the  General 
Manager's  office  of  the  Chicago,  Milwaukee  &  St.  Paul  Kailway,  for 
the  following: 

MILWAUKEE,  July  6, 1875. 
DR.  0.  W.  WIGHT,  State  Geologist, 

SIR:  I  send  you  below  an  account  of  the  different  strata  found  in  putting  down  three 
artesian  wells  on  our  lines  in  this  state.  Yours  Truly,  JOHN  C.  GAULT. 


ARTESIAN   WELL  AT  MILWAUKEE. 


Feet. 


Earth... 170 

Lime  rock , 267 

Shale.... 165 

Second  Limestone 253 

Sandstone  full  of  water 193 


Total  depth 1048 


88  GEOLOGICAL  SURVEY  OF  WISCONSIN. 

AT  WESTERN  UNION  JUNCTION.  Feet. 

Earth 147 

Lime  rock 233 

Shale 200 

Lime  rock 285 

Sandstone 1 100 

Sandy  lime 141 

Struck  St.  Peters  Sandstone 21106 

Depth  of  well 312tj3 


AT  MADISON.  Feet. 

Earth 75 

Sandstone 525 

Shale 4 

Second  Sandstone  . » .  .  185 

Trap  rock  5 


Total  depth 795 


Water  does  not  rise  above  surface  of  ground,  but  it  supplies  a  large  pump,  without 
any  apparent  loss  of  volume. 

MINERAL  SPRINGS.  —  In  addition  to  the  analysis  of  Wisconsin 
spring  waters  given  in  previous  reports  of  the  survey,  two  are  especi- 
ally noteworthy. 

Prof.  C.  F.  Chandler,  Ph.  D.,  Chemist  to  the  New  York  School  of 
Mines,  gives  the  following  analysis  of  the  water  of  the  Beloit  lodo- 
Magnesian  springs : 

Grains  in  1  gallon. 

Chloride  of  Sodium 0.3362 

Bromide  of  Sodium trace. 

Iodide  of  Sodium 0.0049 

Bi-carbonate  of  Soda 0 . 1406 

Bi-carbonate  of  Magnesia 12.2803 

Bi-carbonate  of  Lime 14 . 5196 

Bi-carbonate  of  Iron 0.0396 

Sulphate  of  Lime 0 . 1326 

Sulphate  of  Potash 0.3123 

Phosphate  of  Soda 0.0104 

Alumina 0 . 0590 

Silica 0.7581 

Organic  Matter    trace. 

Total  per  U.  S.  gallon  of  231  cubic  inches 28.5936 


Prof.  Gustavus  Bode,  Chemist  to  the  Wisconsin  Geological  Survey, 
gives  the  following  analysis  of  the  water  of  a  very  remarkable  ar- 
tesian well  at  Sheboygan: 

>  Struck  small  flow. 

a  Pound  15  feet  limestone  in  the  eandatone. 

8  Sandstone  again  to  bottom  mixed  with  red  rock. 


ANNUAL  REPORT  FOR  1875.  89 

One  gallon,  U.  S.  measure,  contains:  — 

Grains. 
Total  quantity  of  Salts 657.8883 


Consisting1  of: 

Bi-carbonate  of  Lime 1 .4945 

Bi-carbonate  of  Magnesia 0.3782 

Chloride  of  Sodium 367.6470 

Chloride  of  Potassium 9.9064 

Chloride  of  Lithium. 0.0244 

Bromide  of  Sodium 1 . 0553 

Iodide  of  Sodium 0.0232 

Sulphate  of  Magnesia 89.3340 

Sulphate  of  Lime 76.1463 

Chloride  of  Calcium , 109.2998 

Sulphate  of  Iron 0.7442 

Alumina 1.0980 

Silica , .  0.7320 


ACKNOWLEDGMENTS.  —  The  State  Geologist  lias  to  thank  in  this 
formal  manner,  the  officers  of  the  Chicago,  Milwaukee  and  St.  Paul 
Railway,  the  officers  of  the  Wisconsin  Central  Railway,  the  officers  of 
the  Wisconsin  Yalley  Railway,  the  officers  of  the  Chippewa  Falls  and 
Western  Railway,  the  officers  of  the  West  Wisconsin  and  the  North 
Wisconsin  Railway,  the  officers  of  the  Green  Bay  and  Minnesota  Rail- 
way, for  free  transportation  of  men  and  materials  in  behalf  of  the  sur- 
vey. The  Wisconsin  Central  and  North  Wisconsin  have  even  put 
trains  at  the  disposal  of  the  chief  geologist,  free  of  cost,  in  order  to 
facilitate  and  expediate  his  work.  Such  generous  liberality  cannot  be 
too  highly  praised.  Acknowledgments  are  also  due  to  Captain  Knapp, 
in  command  of  a  steamboat  on  the  St.  Croix  river,  not  only  for  free 
transportation  of  the  party  of  reconnoissance,  but  for  services  in  pro- 
curing proper  boats  for  ascending  the  river  above  the  falls.  Captain 
Yaughan,  of  Ashland,  also  laid  the  survey  under  especial  obligatioTis 
for  putting  his  tug  boat  at  the  disposal  of  the  undersigned  and  his 
party.  Hotel  keepers  everywhere  in  the  state  have  shown  their  sub- 
stantial good  will  to  the  survey,  by  keeping  men  who  were  working 
in  the  field  at  reduced  rates.  The  American  Express  Company, 
through  the  friendliness  of  its  general  manager  in  this  state,  Mr.  An- 
tisdel,  has  carried  packages  for  the  survey  free  of  cost. 

In  these  various  ways  large  expenditures  of  money  have  been  saved 
to  the  state,  and  the  chief  geologist  has  been  enabled  to  accomplish 
much  more  than  would  otherwise  have  been  possible.  The  people  all 
over  the  commonwealth  have  expressed,  both  verbally  and  by  letter, 
great  interest  in  the  survey,  and  are  looking  forward  with  hopefulness 
of  results  to  the  time  when  its  final  reports  shall  be  published. 

O.  W.  WIGHT,  A.  M.,  M.  D., 

MILWAUKEE,  December  30,  1875.  Chief  Geologist. 


PAET  II. 


GEOLOGY 


OF 


EASTERN    WISCONSIN. 


BY  T.    C.   CHAMBEKLIK 


ACKNOWLEDGMENTS. 

It  is  fitting  that  I  should  acknowledge  in  a  preeminent  degree  my 
obligations  to  the  lamented  Dr.  Lapham,  under  whose  direction  as 
chief  geologist  the  earlier  part  of  the  field  work,  which  forms  the  ba- 
sis of  this  report,  was  performed.  In  addition  to  the  inestimable  value, 
of  such  direction  to  a  young  geologist,  there  was  ever  at  my  disposal 
and  furnished  to  my  needs,  a  large  fund  of  information  concerning 
local  formations  and  the  unwritten  history  of  previous  investigations. 
While  nothing  will  be  found  reported  without  specific  mention  that 
has  not  been  a  matter  of  personal  observation,  it  is  impossible  to  dis- 
cern in  how  far  that  observation  has  been  enriched  by  such  assistance. 

My  acknowledgments  are  also  due  to  those  who  have  been  associa- 
ted with  me  as  assistants  during  the  progress  of  the  work.  Of  these 
especial  mention  is  to  be  made  of  the  accurate  and  efficient  aid  of  Mr. 
L.  C.  Wooster,  who  assisted  in  the  field  work  of  each  season ;  of  Mr. 
F.  II.  King,  who  sustained  that  relation  with  equal  acceptance  during 
two  seasons,  and  of  Mr.  G.  D.  Swezey,  whose  botanical  observations 
are  especially  to  be  noted.  Efficient  assistance  was  also  rendered  for 
shorter  periods  and  special  service  by  Messrs.  K.  D.  "Wright,  Samuel 
Shaw,  S.  E.  Lathrop,  G.  L.  Merriman,  J.  II.  Chamberlin,  and  W.  C. 
Stevens,  and  in  office  work  by  W.  F.  Brown,  I.  M.  Buell,  C.  S.  Bacon, 
C.  S.  Douglas,  and  others.  To  Prof.  R.  F.  Whitfield  I  am  also  in- 
debted for  valuable  suggestions  in  relation  to  paleontological  ques- 
tions. 

For  the  innumerable  courtesies  that  have  been  received  from  citi- 
zens in  the  prosecution  of  the  work,  and  that  in  many  instances  have 
been  of  the  utmost  value,  I  desire  to  express  my  most  sincere  thanks. 
It  would  be  exceedingly  gratifying  to  me  to  be  able  to  make  specific 
mention  of  these  favors,  and  such  acknowledgment  has  been  made  so 
far  as  possible  in  the  manuscript  annual  reports,  but  the  list  has  now 
swollen  to  such  dimensions  as  to  preclude  its  publication  here.  A 
very  just  legal  acknowledgment  has  been  made  in  the  provision  of  the 
law  of  publication  and  distribution,  which  entitles  all  who  have  as- 
sisted in  the  prosecution  of  the  survey  to  a  full  set  of  the  reports,  and 
the  fulfillment  of  that  provision  will  give  me  the  utmost  pleasure. 


EXTENT  OF  THE  DISTRICT. 

The  district  described  in  the  following  chapters  consists  of  the 
counties  of  Rock,  Jefferson,  Dodge,  Green  Lake,  except  that  portion 
lying  on  the  left  bank  of  the  Fox  river,  Winnebago,  Outagamie,  that 
portion  of  Waupaca  which  lies  on  the  left  bank  of  the  Wolf  river ; 
those  portions  of  Shawano  and  Oconto  occupied  by  Paleozoic  rocks, 
and  all  the  counties  lying  east  of  these,  consisting  of  Door,  Kewau- 
nee,  Brown,  Calumet,  Manitowoc,  Sheboygau,.  Fond  du  Lac,  Wash- 
ington, Ozaukee,  Milwaukee,  Waukesha,  Wai  worth,  Racine  and  Ke- 
nosha.  It  constitutes  a  belt  averaging  about  sixty -five  miles  in  width 
and  more  than  one  hundred  and  eighty  in  length,  the  extreme  width 
being  eighty-one  miles,  and  the  extreme  length  a  little  over  two  hun- 
dred. It  includes  nearly  twelve  thousand  square  miles.  The  area 
lies  throughout  its  entire  extent,  adjacent  to  Lake  Michigan,  and  might 
appropriately  be  termed  the  Lake  Border  Region,  were  it  not  that  it, 
includes  so  large  an  area  whose  drainage  is  tributary  to  the  Mississippi. 


PLATEJI 


M  AP 

hiff  t/ic  ,-treri.*  r-ra mined 
by  tlie  several  parties  of  the  Xi 


//     ' 

«>»>x><«<  liine-'i  of   nrcpiinoijtsaitfe 

Bpiine/arif.t  of  districts  e.ranrineri 

r 


PREVIOUS  PUBLICATIONS  RELATING  TO  THE  REGION. 

The  following  is  a  list  of  all  publications  relating  in  any  specific 
way  to  the  region,  that  have  come  to  my  knowledge.  And  as  the  na- 
ture and  limits  of  this  report  preclude,  for  the  most  part,  specific  ref- 
erence to  the  contents  of  these  publications,  either  in  commendation 
or  criticism,  it  is  hoped  that  this  mention  will  be  accepted  as  an  ac- 
knowledgment of  the  credit  due  their  authors: 

Report  of  a  Geological  Reconnoissance,  made  in  1835,  from  the  Seat  of  Government,  by 
Green  Bay,  in  the  Wisconsin  Territory,  to  the  Couteau  de  Prairie.  By  George  W. 
Featherstonhaugh,  Washington.  1836.  8  vo.,  pp.  168. 

On  the  Existence  of  certain  Lacustrine  Deposits,  in  the  vicinity  of  the  Great  Lakes,  •usu- 
ally confounded  with  the  Drift.  By  I.  A.  Lapham.  Am.  Jour,  of  Science,  2d  Se- 
ries, vol.  3,  p.  90.  1847. 

On  the  Geology  of  the  Southeast  Portion  of  Wisconsin,  not  heretofore  surveyed.  By  I. 
A.  Lapham.  Included  in  Foster  and  Whitney's  Report  on  the  Geology  of  the  Lake 
Superior  Land  District.  Part  2d,  pp.  167,  et  seq.  Washington.  1852. 

Geological  Formations  of  Wisconsin.  By  I.  A.  Lapham.  Transactions  of  Wisconsin 
State  Agricultural  Society.  Vol.  2d.  1851,  pp.  122,  et  seq. 

A  Geological  Map  of  Wisconsin.    By  I.  A.  Lapham.    1855. 

Report  of  a  Geological  Survey  of  Wisconsin,  Iowa  and  Minnesota,  and  a  portion  of  Ne- 
braska. By  D.  D.  Owen.  Philadelphia.  1852.  The  chapters  relating  to  this  dis- 
trict are  by  Col.  Whittlesey. 

Annual  Report  of  the  Geological  Survey  of  Wisconsin.  By  James  G.  Percival.  Madi- 
son. 1855.  Ditto,  1856. 

Annual  Report  of  the  Geological  Survey  of  Wisconsin.  By  Edward  Daniels.  Madi- 
son. 1857. 

Report  of  Progress,  on  behalf  of  the  Geological  Commission  of  Wisconsin.  By  James 
Hall.  Executive  Message  and  Documents.  1859. 

Descriptions  of  New  Species  of  Fossils  from  the  Northwestern  States.  By  J.  H.  McChes- 
ney.  Chicago.  1859. 

On  Drift  Cavities,  or  Potash  Kettles  of  Wisconsin.  By  Chas.  Whittlesey.  Proceedings 
American  Association  for  the  Advancement  of  Science.  Vol.  13.  p.  297.  Spring- 
field. 1860. 

Report  of  the  Superintendent  of  the  Geological  Survey  of  Wisconsin.  By  James  Hall. 
January  1,  1861.  Executive  Message  and  Documents. 

Report  of  the  Geological  Survey  of  Wisconsin.  Vol.  1.  By  James  Hall.  Madison. 
January,  1862. 

On  the  Fresh  Water  Glacial  Drift  of  the  Northwestern  States.  By  Charles  Whittlesey. 
Smithsonian  Contributions  to  Knowledge.  Washington.  December,  1866. 


96  GEOLOGY  OF  EASTERN  WISCONSIN. 

Geological  Survey  of  Wisconsin.     1859-1863.     Paleontology.     By  James  Hall. 

Relations  of  the  Niagara  Group.  By  James  Hall.  Report  of  Regents  of  University  of 
New  York. 

On  Western  Boulder  Drift.  By  E.  Andrews.  American  Journal  of  Science.  Part  2. 
Vol.  48.  1869. 

A  New  Geological  Map  of  Wisconsin.    By  I.  A.  Lapham.     Milwaukee.     1869. 

The  Glacial  Features  of  Green  Bay,  of  Lake  Michigan,  with  some  Observations  on  a 
Probable  Former  Outlet  of  Lake  Superior.  By  N.  H.  Winchell.  American  Jour- 
nal of  Sciences  and  Arts.  Vol.  2.  July,  1871. 

United  States  Engineers  Reports  on  the  Surveys  of  Fox  and  Rock  Rivers. 

Geological  Report  of  Michigan.     1869-73.    Dr.  Rominger  on  Paleozoic  Formations. 

Catalogue  of  Plants  Found  in  the  Vicinity  of  Milwaukee.  By  I.  A.  Lapham.  1838. 
12  mo.  pp.  23. 

On  tho  Plants  of  Wisconsin.  By  I.  A.  Lapham.  Proceedings  American  Association  for 
Advancement  of  Science.  Vol.  2.  1850.  pp.  19.  Also  published  in  Transac- 
tions of  Wisconsin  State  Agricultural  Society.  Vol.  2.  1852,  pp.  375,  et  seq. 

Notes  on  the  Woods  of  Wisconsin.  By  P.  R.  Hoy.  Transactions  Wisconsin  State  Ag- 
ricultural Society.  Vol.  2.  1852,  pp.  419,  et  seq. 

The  Grasses  of  Wisconsin  and  the  Adjacent  States.  By  I.  A.  Lapham.  Transactions 
Wisconsin  State  Agricultural  Society.  Vol.  3.  pp.  397,  et  seq. 

The  Forest  Trees  of  Wisconsin.  By  I.  A.  Lapham.  Transactions  Wisconsin  State  Ag- 
ricultural Society.  Vol.  4,  pp.  195,  et  seq. 

Additions  to  the  Flora  cf  Wisconsin.  Transactions  Wisconsin  State  Agricultural  So- 
ciety. Vol.  5.  1858,  p.  417.  Also  vol.  6,  1860,  p.  258. 

Map  of  Wisconsin,  Illustrating  Distribution  of  Timber,  etc.  By  J.  W.  Hoyt.  Transac- 
tions Wisconsin  State  Agricultural  Society,  1860. 

Fauna  of  Wisconsin.  By  I.  A.  Lapham.  Transactions  Wisconsin  State  Agricultural 
Society.  Vol.  2.  1852,  pp.  237,  et  seq. 

Notes  on  the  Ornithology  of  Wisconsin.  By  P.  R.  Hoy.  Transactions  State  Agricul- 
tural Society.  Vol.  2,  1854,  p.  341.  Also,  the  same,  with  additions  in  Proceed- 
ings Academy  Natural  Sciences.  Philadelphia.  Vol.  6.  pp.  304,  381,  425.  1854. 

Quadrupeds  of  Illinois,  Wisconsin,  etc.  By  Robert  Kennicott.  Patent  Office  Reports. 
1856,  p.  52. 


PLATE,  IV 


EASTER  N  WIS  CON  S  IN 


GEOLOGY  OP  EASTERN  WISCONSIN. 


OHAPTEE  I 

TOPOGKAPHY. 

"When  Eastern  Wisconsin  first  emerged  from  the  ocean,  it  doubtless 
presented  an  essentially  plane  surface,  having  a  slight  inclination  to 
the  east  and  southeast.  The  irregularities  which  it  now  presents  are 
due  to  subsequent  changes,  the  results  of  three  classes  of  agents,  act- 
ing at  different  times  and  under  different  conditions. 

1.  During  the  long  ages  between  the  emergence  of  the  land  and  the 
drift  period,  the  streams  were  cutting  their  beds  deeper  and  deeper 
into  the  rock,  and  rendering  the  former  level  surface  more  and  more 
irregular.  The  softer  rocks  were  more  readily  eroded  than  the  harder 
ones,  and  this  helped  to  increase  the  unevenness.  There  was  a  ten- 
dency of  the  streams,  as  far  as  the  slope  favored,  to  follow  the  less 
resisting  belts  of  soft  rock,  and  as  these  run  in  a  northerly  and 
southerly  direction  in  this  region,  the  main  streams  had  that  direction. 
The  little  streams  gathered  into  the  larger  ones  in  a  manner  not  un- 
like that  by  which  the  branches  of  a  tree  are  united  into  the  trunk. 
The  unevenness  of  surface  produced  by  erosion  of  this  nature  pos- 
sesses a  certain  kind  of  system  and  symmetry  readily  recognizable. 
As  this  erosion  occupied  the  time  preceding  the  Glacial  period,  we 
may  conveniently  designate  the  features  produced  by  it  Pre-Glacial. 

"We  have  the  best  example  of  this  kind  of  surface  configuration  in 
the  Lead  region,  over  which  the  drift  forces  did  not  act,  and  which 
has  not  been  resubmerged,  so  that  we  have  the  results  of  this  class  of 
action  pure  and  simple.  As  we  proceed  eastward  into  the  region  of 
drift  action  in  the  central  part  of  the  state,  these  features  arc 
modified  more  and  more  by  the  results  of  glacial  action,  until  in  east- 
ern "Wisconsin  they  become  wholly  obscured,  except  in  their  grander 
outlines. 

Wis.  SUB.— 7 


98  GEOLOGY  OF  EASTERN  WISCONSIN. 

2.  The  modifications  of  the  surface  constituting  this  first  class  of 
topographical  features  were  produced  by  running  water,  those  of  the 
second  class,  which  were  produced  next  in  order  of  time,  were  formed 
by  ice  in  the  form  of  glaciers,  it  is  confidently  believed,  and  by  the 
agencies  brought  into  action  through  their  melting.     The  work  of  the 
ice  was  two-fold:  first,  in  the  leveling  of  the  surface  by  planing  down 
the  hills  and  filling  up  the  valleys;  and  second,  in  the  creation  of  a 
new  uneven  surface,  by  heaping  up  in  an  irregular  and  promiscuous 
manner  the  clay,  sand,  gravel  and  bowlders  it  had  formed,  thus  giving 
the  surface  a  new  aspect. 

Among  the  features  produced  by  the  action  of  the  ice,  are  parallel 
ridges  sometimes  miles  in  length,  having  the  same  direction  as  the  ice 
movement,  hills  of  rounded  flowing  contour  sometimes  having  a  lin- 
ear arrangement  in  the  direction  of  glacial  progress,  mounds  and 
hummocks  of  drift  promiscuously  arranged  on  an  otherwise  plane 
surface,  oval  domes  of  rock  (roches  moutonees),  sharp  gravel  ridges, 
often  having  a  tortuous  serpentine  course,  transverse  to  the  drift 
movement,  peculiar  depressions  known  as  "  kettles,"  and  half  sub- 
merged rock  gorges,  known  as  fiords,  all  of  which  will  be  considered 
more  fully  in  describing  the  minor  topographical  features  of  the  re- 
gion, and  in  discussing  the  Quaternary  formations. 

The  melting  of  the  ice  mass  gave  rise  to  swollen  lakes  and  flooded 
rivers,  which  eroded  at  some  points  and  filled  up  at  others,  and  so 
still  farther  modified  the  face  of  the  country.  All  these  peculiarities, 
being  the  result,  directly  or  indirectly,  of  the  ice  action,  may  be  de- 
nominated Glacial  features. 

3.  Subsequent  to  the  Glacial  period,  the  wearing  action  of    the 
streams  was  resumed,  but  under  somewhat  new  conditions.     In  addi- 
tion to  this,  there  occurred  a  depression 'of  the  land  toward  the  north 
of  several  hundred  feet,  attended  by  an  increased  volume  of  water  in 
the  lakes,  by  which  nearly  one-half  of  the  district  was  submerged. 
The  advancing  waters  of  this  period  leveled  down  many  of  the  surface 
irregularities,  and  while  the  land  was  submerged  the  "  red  clay"  was 
deposited  which  still  further  leveled  the  surface.     After  the  land 
arose  again  from  the  water,  the  streams  resumed  their  cutting,  and  as 
the  clay  was  soft,  they  rapidly  eroded  deep,  wide  gorges,  leaving 
abrupt  terraces  on  either  side.     The  results  of  the  these  agencies  pro- 
duced peculiarities  in  the  surface  contour  that  may,  following  out  our 
plan,  be  called  Post-Glacial  features. 

To  the  three  agencies,  lake  action,  ice  and  running  water,  assisted 
slightly  by  winds,  the  topographical  peculiarities  of  the  district  are 
chiefly  due.  There  is  no  evidence  of  violent  eruptions,  upheavals  or 


TOPOGRAPHY.  99 

outbursts.  There  was  indeed  tlie  gradual  elevation  and  depression  of 
the  surface  and  probably  some  little  flexure  of  the  crust,  and  there 
are  at  two  or  three  points,  indications  of  faulting;  but  in  general,  the 
region  has  been  free  from  violent  agitation,  and  owes  none  of  its  sali- 
ent topographical  features  to  such  causes. 

Having  thus  briefly  considered  the  general  methods  by  which  the 
present  aspect  of  the  country  was  produced,  we  may  now  more  satis- 
factorily examine  its  special  features,  and  if  the  reader  will  have  re- 
course to  Plate  IV  of  this  volume,  and,  for  minor  details,  to  the 
accompanying  atlas,  it  will  relieve  us  mutually  of  the  wearisomeness 
of  mere  elementary  geographical  details,  while  it  contributes  to  a 
clearer  and  more  vivid  understanding  of  the  subject. 

]STo  part  of  Wisconsin  can  properly  be  said  to  be  mountainous,  nor 
does  it,  over  any  considerable  area,  sink  to  a  dead  level.  It  presents 
the  golden  mean  in  a  gently  undulating  diversified  surface,  readily 
traversible  in  all  directions  by  the  various  highways  of  commu- 
nication. The  eastern  district  under  consideration  contains  the  more 
level  portions  of  the  state,  but  presents  at  the  same  time  much  of  di- 
versity and  many  most  interesting  topographical  features. 

Setting  aside  minor  details,  the  state  presents  two  general  slopes, 
a  short,  abrupt  declivity  northward  to  Lake  Superior,  and  a  long, 
gentler  incline  southward.  Through  the  center  of  this  southward 
slope  there  extends  a  moderate  elevation  —  a  low  anticlinal  axis  — 
giving  a  southeasterly  and  southwesterly  inclination  to  the  strata  on 
either  side.  The  district  under  consideration  is  wholly  confined  to 
the  southeasterly  slope. 

The  symmetry  and  simplicity  of  this  system  is  however  traversed 
in  a  peculiar  manner  by  a  diagonal  valley  occupied  by  Green  Bay 
and  the  Fox  and  Wisconsin  rivers.  This  feature  of  the  general  sur- 
face of  the  state  enters,  in  an  interesting  way,  into  the  topography  oil 
our  district,  and  from  its  commercial  importance  demands  attention. 
This  valley,  including  its  extension  into  Michigan,  is  occupied  by  the 
waters  of  Green  Bay  for  about  one  hundred  miles,  with  an  average 
breadth  of  about  twelve  miles.  The  bay  projects  into  Wisconsin 
about  seventy  miles  beyond  Porte  des  Morts  at  the  extremity  of  the 
peninsula,  and  about  forty-five  miles  beyond  the  mouth  of  the  Me- 
nomonee  river,  which  forms  the  state  boundary. 

This  valley  is  abruptly  limited  on  the  east  side  by  precipitous  rocky 
cliff's  rising  from  100  to  200  feet  above  the  Bay.  From  the  crest  of 
these  cliffs,  the  land  slopes  toward  Lake  Michigan.  On  the  opposite  or 
wes-t  side  of  the  valley,  the  surface  rises  very  gradually  for  20  to  30 
miles,  beyond  which  the  slope  becomes  somewhat  steeper.  The  Bay 


100  GEOLOGY  OF  EASTERN  WISCONSIN. 

has  a  trend  of  about  S.  35°  "W.  Following  up  the  valley  in  this  direc- 
tion, it  presents  the  same  characteristics,  bounded  by  an  abrupt  wall 
of  rock  on  the  east,  and  gently  sloping  upward  to  the  west.  It  rises 
somewhat  rapidly,  so  that  when  Lake  Winnebago  is  reached,  an  eleva- 
tion of  169^-  feet,  canal  survey,  or  162  feet,  railroad  survey,  has  beeu 
attained.  This  lake  strikingly  resembles  Green  Bay  in  the  nature  of 
its  eastern  and  western  shores.  Its  trend,  however,  is  nearly  due  north 
and  south,  and  if  we  follow  on  in  this  new  direction,  the  valley  leads 
up  over  the  watershed  between  the  Mississippi  and  St.  Lawrence  ba- 
sins, into  the  valley  of  Rock  river.  This  extension  of  the  Green  Bay 
valley  will  be  noticed  farther  on. 

For  the  present,  however,  we  are  considering  the  diagonal  valley  — 
the  topographical  and  drainage  basin  —  which  has  its  extension  in  the 
valley  of  the  Upper  Fox  river.  Like  the  preceding,  this  portion  of  tho 
valley  has  its  more  abrupt  slope  on  the  south  side,  but  this  is  far  lesa 
conspicuous  than  before,  nor  do  we  find  the  same  broad,  level  tract  on 
the  opposite  side.  These  differences  are  due  partly  to  the  fact  that 
the  valley,  in  this  portion,  crosses  the  geological  formations  obliquely, 
whereas,  in  the  lower  portion,  it  followed  their  trend,  and  partly  to 
the  fact  that  here  the  drift  movement  was  across  the  valley  from  east- 
ward to  westward  to  a  considerable  extent.  This  valley  undoubtedly 
had  an  existence  before  the  glacial  epoch,  and  during  that  period  it 
was  probably  more  filled  than  eroded. 

The  Fox  river,  in  this  portion  of  its  course,  has  a  much  less  rapid 
descent  than  between  Lake  Winnebago  and  Green  Bay,  a  circumstance 
greatly  favoring  its  improvement  and  navigation.  The  Upper  Fox 
descends  40  feet  in  an  air-line  distance  of  about  60  miles,  or  a  little 
more  than  100  miles  along  its  meanderings,  while  the  Lower  Fox  de- 
scends 162  (169£)  feet  in  half  that  distance. 

The  valley  leading  south  from  Lake  Winnebago,  which  has  beeu 
alluded  to  as  an  extension  of  the  Green  Bay  valley,  and,  as  will  here- 
after be  seen,  is  in  many  respects  entitled  to  be  so  considered,  rises 
140  feet  in  15  miles.  These  facts,  supported  as  they  are  by  many 
others  of  similar  import,  show  that  the  diagonal  valley  under  consid- 
eration is  not  a  fanciful  conception,  but  a  well  characterized,  if  not 
obvious,  fact. 

The  commercial  importance  of  this  valley  in  presenting  suitable 
conditions  for  the  establishment  of  water  communication  between  the 
Mississippi  and  the  great  lakes,  has  awakened  a  deep  interest  among 
leading  citizens  of  this  and  adjoining  states,  and  public  attention 
has  been  so  thoroughly  turned  toward  it,  and  the  prospect  of  realiza- 
tion is  so  good,  and  so  immediate,  that  so  far  as  the  people  of  the  state 


TOPOGRAPHY. 


101 


are  concerned,  it  would  need  little  discussion  here,  even  if  the  limits 
of  my  field  comprehended  its  entire  extent  and  brought  the  whole 
of  the  subject  under  consideration.  But  it  deserves  to  be  here  record- 
ed for  the  information  and  guidance  of  capitalists  abroad,  that  for  a 
moderate  expenditure  this  remarkable  natural  feature  can  be  made  to 
yield  an  important  avenue  of  transportation. 

In  this  connection  the  attention  of  capitalists  is  invited  to  the  facts 
given  subsequently  in  relation  to  the  water  power  of  the  Lower  Fox 
river,  bearing  in  mind  that  grain  bearing  vessels  will  offer  return 
transportation  at  the  most  reasonable  rates,  thus  placing  manufactur- 
ing establishments  in  the  most  advantageous  relation  to  the  thousands 
of  miles  of  rich  territory  along  the  Mississippi  and  its  tributaries,  and 
the  still  other  thousands  of  miles  of  shore  line  around  the  great  lakes. 
The  enterprise  for  the  improvement  of  this  channel  of  communication, 
under  the  auspices  of  the  general  government,  is  already  (1876)  far 
advanced. 

It  has  been  already  remarked  that  the  valley  from  Green  Bay  to 
Lake  Winnebago  is  exceedingly  abrupt  on  the  east,  and  very  slightly 
ascending  on  the  west.  The  persistence  of  this  peculiarity  for  so  great 
a  distance  points  to  some  general  cause.  This  is  readily  found  in  the 
nature  of  the  rock  from  which  the  valley  was  eroded.  The  strata  in 
this  portion  of  the  state  dip  to  the  eastward.  Three  groups  of  beds 
are  concerned  in  the  formation  of  the  valley.  The  uppermost  one, 
which  forms  the  cliffs  on  the  east  side,  consists  of  hard,  thick-bedded 
magnesian  limestone,  belonging  to  the  Niagara  period.  Beneath  this 
lies  a  series  of  clays,  soft  shales,  and  limestones,  very  easily  eroded  by 
water,  forming  the  Cincinnati  group,  and  below  this  again  is  a  hard, 
thick-bedded  dolomite,  known  as  Galena  limestone,  which  forms  the 
bottom  of  the  valley  and  its  western  slope,  as  shown  in  the  accom- 
panying figure  : 

FIG.  1. 


1.  Galena  limestone.     2.  Cincinnati  shale.     3.  Niagara  limestone.     1 — 2.  Gre^n  Bay  valley. 

It  becomes  evident  enough  then,  from  these  facts  and  from  an  in- 
spection of  the  valley,  that  it  was  formed  by  the  wearing  away  of  the 
softer  strata,  leaving  the  harder  ones  above  projecting  in  mural  cliffs. 
This  eroding  action  is  still  going  on,  and  to  some  extent  is  greatly  fa,- 


102  GEOLOGY  OF  EASTERN  WISCONSIN 

cilitated  bj  numerous  springs  that  issue  from  the  upper  surface  of 
the  clay  and  shale,  keeping  them  soft  and  assisting  in  wearing  them 
down.  The  dip  of  the  rocks  tended  to  keep  the  stream  hard  against 
the  soft  stratum,  and  so  hastened  its  removal. 

There  is  abundant  reason  for  believing  that  this  process  had  far 
advanced  before  the  glacial  period,  and  had  already  formed  so  consid- 
erable a  valley  as  to  influence  the  glacial  movement.  During  the 
latter  part  of  that  period,  at  least,  the  ice  mass  moved  southward  up 
the  valley,  modifying  its  sides  and  polishing  its  rock  bottom  in  the 
most  beautiful  manner.  Subsequently  the  valley  was  partially  filled 
with  red  clay,  without  however  affecting  its  general  features.  The 
strati  graphical  relations  of  this  valley  are  then  most  conspicuous. 
If,  keeping  this  prominently  in  mind,  we  follow  up  the  valley,  we  are 
led  southward  from  Lake  Winnebago  to  what  was  formerly  Lake 
Horicon,  now  drained  to  a  marsh,  where  the  head  waters  of  the  Rock 
river  gather  together  and  flow  southward  to  the  Mississippi.  We 
have  then  crossed  the  watershed  between  the  great  St.  Lawrence  and 
Mississippi  basins;  and  yet  on  the  very  divide  itself  we  find  the  pe- 
culiar character  of  the  valley  still  conspicuous.  The  watershed  in 
the  trough  of  the  valley  is,  in  round  numbers,  200  feet  above  Lake 
Michigan,  while  on  either  side  the  surface  rises  to  more  than  twice 
that  elevation. 

The  Horicon  basin  is  only  a  repetition  of  that  of  Lake  Winnebago, 
overlooked  by  the  same  line  of  cliffs  on  the  east,  and  scarcely  confined 
by  the  gentle  rise  on  the  west.  Descending  the  Rock  river  valley, 
these  features  are  still  discernible,  but  become  more  and  more  ob- 
scured by  the  heavy  drift  accumulation  of  this  region,  until  in  the 
southern  tier  of  counties  they  are  almost  entirely  concealed  by  a  great 
drift  ridge,  a  glacial  moraine,  hereafter  to  be  described,  which 
stretches  entirely  across  the  valley  and,  combined  with  other  elements, 
gives  it  a  new  character.  The  river  has  removed  from  the  eastern 
side  of  the  valley  to  a  more  central  position,  and  from  it  there  arise 
diversified  undulating  slopes  on  either  side. 

The  course  of  the  Rock  river  through  this  valley  is  interesting  and 
for  convenience  may  here  be  considered,  in  lieu  of  its  appropriate 
place.  From  Horicon  marsh  southward,  it  follows,  as  closely  as  the 
drift  accumulations  will  permit,  the  ledge  of  JSTiagara  limestone  above 
mentioned  until  about  opposite  Oconomowoc,  when  it  turns  abruptly 
and  flows  to  the  northwest,  until  it  reaches  Watertown,  where  it  bends 
again  suddenly  to  the  southward  and  follows  this  course,  bearing 
westward,  till  it  leaves  the  state.  The  sigmoid  flexure  thus  formed  is 
apparently  due  to  drift  accumulations.  Were  these  removed,  there  is 


TOPOGRAPHY.  103 

little  doubt  that  the  stream  would  follow  its  course  along  the  strike  of 
the  formations,  at  least  as  far  as  the  moraine  in  Wai  worth  county. 
Beyond  that  point  the  drift  is  so  deep  as  to  preclude  any  knowledge 
of  the  configuration  of  the  rock  surface. 

It  is  interestino-  to  notice  that  this  river,  which  has  been  following 

O  *  O 

the  trend  of  a  soft,  easily  eroded  formation  —  the  Cincinnati  shale  — 
from  which  it  is  now  forced  by  drift,  passes  across  the  Galena  and 
Trenton  limestones  and  makes  its  bed  in  the  next  lower  soft  forma- 
tion, the  friable  St.  Peters  sandstone,  which  it  follows,  until  it  leaves 
the  state. 

Considering  the  Rock  river  valley  as  an  extension  of  that  of  Green 
Bay,  the  two  forming  one  great  excavated  trough,  the  elevations  it 
attains  become  matters  of  much  geological  and  commercial  import- 
ance. At  the  north,  it  finds  in  Green  Bay  the  level  of  Lake  Michi- 
gan and,  as  has  been  previously  remarked,  rises  somewhat  rapidly 
about  1TO  feet  to  Lake  Winnebago.  Throughout  the  length  of  that 
lake,  a  distance  of  thirty  miles,  it  is  essentially  level.  From  its 
southern  extremity,  the  valley  again  rises  about  140  feet  to  the  wat- 
ershed, making  its  greatest  elevation  a  little  over  300  feet.1  The 
former  Lake  Horicon  was  285  feet  above  Lake  Michigan.  From  this 
point  a  gentle  declivity  brings  the  valley  down  to  150  feet,  at  Beloit, 
on  the  state  line.  It  continues  its  moderate  descent  till  it  joins  the 
Mississippi,  where  it  is  about  50  feet  below  Lake  Michigan.  This 
Illinois  extension  of  the  valley  differs,  however,  somewhat  widely  iii 
geological  and  topographical  features  from  the  portion  in  Wisconsin. 

The  commercial  importance  of  the  foregoing  facts  is  very  consid- 
erable as  now  realized,  but  is  far  greater  in  its  future  possibilities. 
It  furnishes  important  facilities  for  both  land  and  water  communica- 
tion. The  sagacious  proprietors  of  the  Chicago  &  Northwestern 
Railway  early  perceived  this  and  located  nearly  200  miles  of  their 
road  in  this  valley,  thus  securing  an  easy  grade  along  a  line  of  im- 
portant towns,  supported  by  an  exceedingly  rich  agricultural  region, 
and  possessing  some  of  the  finest  water  powers  of  the  interior. 

Water  communication  is  utilized  to  some  extent,  but  the  great  pos- 
sibilities in  this  direction  lie  yet  undeveloped.  In  the  year  1866,  a 
survey  of  this  valley  from  Fond  du  Lac  to  the  Mississippi  was  au- 
thorized by  the  general  government  and  executed  by  Col.  James  Wor- 
rall,  under  the  direction  of  Gen.  J.  EL  Wilson,  having  for  its  object 
the  determination  of  the  practicability  of  establishing  a  capacious 

1  All  elevations  in  this  report,  unless  otherwise  designated,  signify  altitude  above  Lake 
Michigan,  which,  awaiting  more  accurate  measurements,  is  considered  578  feet  above 
the  ocean. 


104:  GEOLOGY  OP  EASTERN  WISCONSIN. 

channel  of  water  communication  between  the  Mississippi  and  the 
northern  lakes.  Important  facts  developed  by  that  survey  may  be 
found  in  Ex.  Doc.  No.  15,  of  the  House  of  Representatives,  40th 
Congress,  and  should  not  be  forgotten  by  an  enterprising  people. 

Returning  from  this  digression,  it  is  to  be  remarked  that  the  diag- 
onal valley  previously  described,  and  this  Rock  river,  Green  Bay  val- 
ley, unite  at  the  north  and  join  the  great  depression  occupied  by  Lake 
Michigan.  The  bed  of  this  great  lake  is  excavated  chiefly  from  the 
soft  rocks  of  the  Devonian  age,  and  has  its  axis  parallel  to  the  strike 
of  the  formations.  The  western  edge  of  the  lake  rests  upon  the  Ni- 
agara dolomites,  but  the  dip  of  the  formation  is  greater  than  the 
slope  of  the  lake  bed,  so  that  this  formation  is  probably  overlaid  near 
the  western  edge  of  the  lake  by  the  upper  formations. 

This  great  submerged  valley  possesses  one  of  the  main  features 
that  characterize  the  Green  Bay  valley,  that  of  having  a  more  abrupt 
slope  on  the  east.  At  least  this  is  true  of  the  northern  portion  accord- 
ing to  the  lake  survey  charts,  for  which  I  am  indebted  to  the  kindness 
of  Gen.  0.  B.  Comstock.  This,  however,  is  not  a  conspicuous  fact, 
and  the  eastern  shore  is  far  from  being  precipitous.  The  eastern  line 
of  Wisconsin  would,  if  traced  on  the  bottom  of  Lake  Michigan,  lie 
almost  wholly  below  the  sea  level.  The  extent  to  which  Lake  Michi- 
gan occupies  the  territory  of  the  state  and  its  nearly  constant  level, 
make  its  surface  our  most  convenient  datum  plane  in  giving  elevations 
and  discussing  topographical  features.  The  elevation  of  the  surface 
of  the  lake  above  the  sea  level,  that  has  been  adopted  in  the  progress 
of  the  survey,  is  578  feet.  In  the  report  of  the  survey  of  Rock  river, 
576  feet  is  given,  and  Gen.  Comstock  informs  me  that  the  lake  survey 
use  at  present  581  feet  above  mean  tide  at  New  York.  The  series  of 
levels,  now  being  run,  will,  when  completed,  give  for  the  first  time  an 
accurate  determination  of  the  level  of  the  great  lakes. 

The  erosion  of  the  great  valleys  we  have  now  considered  left  of 
necessity  adjacent  slopes  and  dividing  ridges.  North  of  the  Fox 
river  a  very  large  area  is  included  in  a  southerly  and  southeasertly 
incline,  the  drainage  of  which  is  tributary  to  that  river.  This  is  indi- 
cated clearly  by  the  general  course  of  the  Wolf,  Oconto,  Peshtigo  and 
Menomonee  rivers  and  their  branches.  On  the  west  side  of  Rock 
river  there  is  a  similar  slope  tributary  to  it.  But  the  most  conspicu- 
ous elevation  in  the  district  is  the  extensive  ridge  that  lies  immedi- 
ately east  of  the  valleys  of  Green  Bay  and  Rock  river,  and  which  has 
already  been  cursorily  mentioned  in  the  descriptions  of  those  valleys. 

A  glance  at  the  course  of  the  rivers  of  this  region  shows  that  the 
summit  of  this  elevation  is  immediately  adjacent  to  the  valleys  men- 


TOPOGRAPHY.  105 

tioned.    Its  average  elevation  above  Lake  Michigan  varies  from  about 

o  o 

400  feet,  in  the  south  and  central  portions,  to  200  feet,  at  the  north, 
while  isolated  points  considerably  exceed  these  figures.  From  this 
crest  the  surface  slopes  eastward  to  Lake  Michigan,  and  onward  under 
its  waters  down  to  and  below  the  sea  level.  With  an  unessential  ex- 
ception, this  slope  is  everywhere  underlaid  by  the  Niagara  limestone, 
to  the  dip  of  which,  and  the  softness  of  the  underlying  shale,  the 
ridge  owes  its  origin.  Indeed,  the  ridge  is  simply  the  projecting  edge 
of  the  inclined  Niagara  strata.  At  the  south,  where  this  eastward 
slope  enters  the  state  from  Illinois,  it  is  about  forty  miles  wide.  It 
retains  this  amplitude  for  upwards  of  100  miles,  extending  in  an 
almost  due  north  course,  beyond  which  it  curves  more  rapidly  to  the 
eastward,  and  gradually  narrows  till  the  limiting  waters  of  Lake  Mich- 
igan and  Green  Bay  on  either  side  meet  and  mingle  through  Porte 
des  Morts.  But  in  fact  it  does  not  end  here.  As  a  submerged  ridge 
it  extends  onward  to  Michigan,  its  crest  appearing  as  a  line  of  islands, 
stretching  across  to  the  peninsula  east  of  Big  Bay  de  Noquet,  which 
presents  similar  features  due  to  the  same  cause. 

Without  destroying  the  truth  of  what  has  been  said  of  this  east- 
ward sloping  rock-ridge,  the  region  presents  a  secondary  topographi- 
cal feature  of  no  insignificant  importance. 

It  consists  of  a  line  of  immense  drift  hills,  superimposed  upon 
the  terrane  just  described,  and  known  as  the  Potash  ITettle,  or  Pots 
and  Kettles  Range.  As  the  term  "  Potash  "  has  now  no  special  sig- 
nificance, it  will  be  dropped  from  this  report.  At  the  south  these 
drift  hills  rest  directly  upon  the  summit  of  the  rock-ridge,  their 
added  height  reaching  an  altitude  of  from  400  to  800  feet  above  Lake 
Michigan.  To  the  northward,  however,  the  drift  moraine  has  a  some- 
what more  easterly  trend  than  its  indurated  companion,  and  creeps 
down  the  eastern  slope  of  the  latter,  until  it  ends  in  Kewaunee  county, 
midway  between  the  shore  of  Lake  Michigan  and  the  rock-crest  that 
overlooks  Green  Bay.  This  modifies,  somewhat,  the  simplicity  of 
contour  that  would  otherwise  be  presented,  but  owing  to  the  great  ir- 
regularity of  the  drift  accumulation,  the  streams  find  their  way  across 
it,  and  the  drainage  system  of  Lake  Michigan  is  not  essentially  affect- 
ed by  it.  In  Walworth  county  a  branch  from  this  drift  ridge  extends 
westward,  crossing  the  Rock  river,  beyond  which  it  curves  to  the 
northward,  and  passes  beyond  the  limits  of  my  district.  The  effect 
of  this  upon  the  features  of  the  Rock  river  valley  has  already  been 
noted. 

These  then  are  the  salient  topographical  features  of  the  district, 
the  great  Lake  Michigan  basin,  the  Green  Bay  valley,  with  its  two- 


106  GEOLOGY  OF  EASTERN  WISCONSIN. 

fold  extension  in  the  Upper  Fox  and  "Wisconsin  river  valleys,  and  in 
the  Rock  river  basin,  and  their  attending  slopes  and  ridges. 

If  we  descend  to  minor  features,  a  large  number  of  most  interesting 
phenomena  will  be  presented.  As  these,  however,  are  chiefly  due  to 
erosion  and  to  drift  accumulations,  they  may  most  intelligently  be 
considered  in  connection  with  the  drainage  system  and  the  glacial  for- 
mations. 

Elevations.  The  following  elevations  constitute  a  more  specif- 
ic class  of  topographical  data.  They  will  be  of  great  value  in  ?nak- 
ing  estimates  for  Artesian  wells,  a  subject  which  possesses  very  gieat 
importance  in  this  region,  and  in  locating  preliminary  lines  of  rail- 
road, in  which  respect  they  have  already  proved  serviceable,  and  in  vari 
ous  other  ways.  The  elevations  of  railroad  stations,  and  in  manj 
cases  of  intermediate  points  on  the  line,  are  those  furnished  me  by 
Dr.  Lapham,  from  the  railroad  surveys.  To  the  same  source,  also,  1 
am  indebted  for  the  altitudes  of  the  Oconomowoc  lakes,  and  some 
other  points.  The  elevations  along  the  line  of  the  proposed  Chicago 
and  Midland  railroad  are  from  the  survey  of  Mr.  F.  J.  Stariu,  who 
kindly  placed  the  profiles  at  my  service,  which  have  proved  of  much 
use  in  other  ways.  Elevations  on  the  Peshtigo  river  were  gener- 
ously furnished  by  Mr.  Paul  Wood,  civil  engineer  of  the  Peshtigo 
Company.  A  few  have  also  been  taken  from  other  trustworthy 
sources.  These  being  the  results  of  actual  leveling,  by  competent  en- 
gineers, are  a  very  close  approximation  to  the  actual  elevations.  The 
remainder  are  the  results  of  observations  with  aneroid  barometers, 
and  are  liable  to  more  considerable  errors,  because  the  nature  of  the 
instrument  does  not  permit  so  great  precision,  and  more  especially 
because  of  the  fluctuations  of  the  atmosphere,  for  which,  in  a  series  of 
observations  made  in  connection  with  and  subordinate  to  geological 
field  work,  it  is  impossible  to  make  altogether  accurate  corrections. 
A  very  large  number  of  observations  were  made  which  are  not  thought 
worthy  of  publication,  because  changes  in  the  weather  and  other  cir- 
cumstances rendered  them  unreliable,  and  in  using  those  given  it  will 
be  judicious  to  leave  a  liberal  margin  for  variation  due  to  changes  in 
the  pressure  of  the  atmosphere,  which  could  not  be  detected.  The  la- 
borious work  of  reducing  the  barometrical  observations  was  chiefly 
performed  by  Messrs,  L.  C.  "Wooster,  G.  D.  Swezey,  J.  H.  Chamber- 
lin  and  C.  S.  Bacon.  The  elevations  for  Milwaukee  county  are  the 
results  of  a  special  and  very  full  series  of  observations  made  by  Chas. 
Lapham,  which  the  importance  of  that  region,  as  a  railroad  center, 
seemed  to  warrant. 


TOPOGRAPHY. 


107 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN. 

(For  the  elevation  above  the  ocean,  add.  578  foot.) 


Ahnapee.    T.  25,  R.  25  E.  Feet. 

Sec.  5,  S.  W.  qr.,    -  -      60 

Bank  S.  of  Almapee,     -  60 

Three  miles  S.  W.  of  Almapee,  -     122 

Angelica.    T.  26,  R.  18  E. 

Sec.:*),       -  -    285 

Ashforrt.    T.  13,  R.  18  E. 

Sec.    2,  N.  Line,  441 

2,  average,     -  -    516 

3,  R.  R.  cut,        -  459 
11,  N.  E.  qr.,  - 

13,  center,  466 

23,  Elmore  Village,  -    421 

23,  Surface  of  Kettle  Formation,  444 

24,  W.  side  river,  322 
Auburn.    T.  13,  R.  19  E. 

Sec.    8,  center  N.  hf.f        -  -    490 
New  Cassel  bridge, 

New  Cassel  depot,  -  -     466 

Sec.  30,  Five  Points,     -  468 

30,  R.  R.  crossing,       -  -    409 

32,  S.  E.  qr.,  Milwaukee  river,    376 
Avon.    T.  1,  R.  10  E. 

Sec.    5,  N.  E.  qr.,        -  272 

5,  S.  E.  qr.,  stream,  -  -     192 

9,  S.  W.  qr.,        -  320 

13,  -    327 

13,  Bottom  of  Galena,      -  330 

18,  S.  E.  corner,  -    318 

22,  S.  W.  qr.,       -  245 

23,  S.  W.  qr.,  slough,  -     171 
Aztalan.    T.  7,  R.  14  E. 

Sec.  7,  S.  W.  qr.,             -  -    251 

17,  Village,          -  276 

18,  N.  E.  qr.,  -  -    297 
18,  Marsh,  252 
20,  S.  E.  qr.,  river  bank,  -    226 
20,  S.  E.  qr.,  water  level,-  210 

Barton.    (See  Kewaskum.) 
Beaver  Dam.    T.  11,  R.  14  E. 

Sec.    2,  near  mid.  W.  line,  -    277 

2,  center  S.  E.  qr.,  creek,  268 

3,  N.,E.  qr.,  -  -    327 
Beaver  Dam  Lake,  282 

Sec.    7,  S.  W.  qr.,  marsh,  -    284 

8,  near  center  N.  W.  qr.,  300 

10,  N.  W.  qr.,  ridge,  -  -    320 
Beaver  Dam.    T.  12,  R.  14  E. 

Beaver  Dam  Station,  -    340 

Sec.  34,  mid.  S.  E.  qr.,  R.  R.,  317 

Belgium.    T.  12,  R.  22  E. 

Sec.    2,  N.  line,           -           -  145 

3,  S.  line,        -            -  -     145 

10,  N.  line,            -            -  145 

10,  S.  line,        -            -  -     152 

15,  N.  line,           -           -  152 

22,  N.  line,      -            -  -    153 

28,  N.  line,  156 

33,  N.  line,  Deckers,    -  -    154 
Bellevue.    T.  23,  R.  21  E. 

Sec.  15,  mid.  W.  line,        -  -     136 

20,  S.  E.  qr.,  stream,        -  28 


Beloit.    T.  1,  R.  12  E.  Feet. 

Sec.    3,  S.  W.  qr.  of  S.  W.  qr.,  196 

6,  near  center  W.  line,  -    200 

6,  S.  W.  corner,  hill,  -            309 

10,  E.  line  N.  E.  qr.,  -     152 

10,  N.  E.  qr.,        -  180 

10,  near  center,  -     273 

10,  S.  E.  qr.,        -  -            200 

10,  S.  line,  S.  E.  qr.,  -     302 

17,  near  center,     -  -            314 

17,  N.  W.  qr.,              -  -    228 

18,  S.  E.  corner,    -  -            225 

18,  S.  line,  hill,  -    260 

19,  center  W.  hf.,  264 

26,  N.  W.  qr.,             -  -     193 

27,  near  center,     -  197 

28,  mid.  S.  line,  -    251 
28,  Hyde's  place, 

28,  Summit,  Hyde's,  -            275 

29,  N.  E.  qr.,  creek,  -            189 

30,  S.  E.  comer,           -  -     167 

31,  center,  creek,  144 

33,  mid.  W.  line,  -    210 

34,  N.W.  qr.,  Hanchett's  quarry,  213 
34,  S.  E.  qr.  of  N.  W.  qr.,  201 

34,  mid.  W.  line,  -           236 

35,  S.  E.  qr.,  -     161 

36,  near  center  S.  E.  qr.,  -           176 
S.  line  College  Campus,      -  -    192 
lodo-Magnesian  springs,  177 

Bloomfleltl.    T.  1,  R.  18  E. 

Sec.  6,  N.hf.,  -  -  345 

35,  N.  E.  qr.,  -  -  2-54 

35,  S.  E.  qr.,  -  -  264 

Genoa  Station,  -  264 
Bradford.  T.  2,  R.  14  E. 

Hill  W.  of  Fairchild,  -  -  325 
Brighton.  T.  2,  R.  20  E. 

Sec.  18,  N.  hf.,  250 
Brillion.  T.  20,  R.  20  E. 

Sec.   6,  N.  E.  corner,  -    175 

6,  mid.  S.  line  S.  E.  qr.,  211 

7,  Forrest  Junction,   -  -    250 

15,  near  mid.  W.  line,  -            255 

16,  near  mid.  S.  line    -  -    249 
18,  near  mid.  N.  line,  -            250 

18,  near  mid.  S.  line,  -  -    267 

19,  mid.  S.  line  S.  W.  qr.,  250 

22,  mid.  W.  line  N.  W.  qr.,   -    250 

23,  near  S.  W.  corner,  -            229 

25,  W.  line,     -           -  -    248 

26,  mid.  N.  line  N.  W.  qr.,         227 

30,  mid.  W.  hf.,          -  -    230 

31,  mid.  W.  hf.,  -  -           238 
Bristol.    T.  1,  R.  21  E. 

Sec.  5,  Branch  of  Eau  Pleine,        -     149 

Bristol  station,  -            191 

Sec.  8,  N.  W.  qr.,  -            -  -    214 

9,  center,river,      -  -            147 

9,  W.  line,       -            -  -    154 

Woodworth  station,    -  170 

Sec.  12,  center,        -           -  -    128 


108 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN — continued. 


Bristol.    T.  1,  R.  21  E.  — (con.)         Fe>t 

Sec.  19,  N.  W.  qr.,      -  230 

Brooktield.    T.  7,  R.  20  E. 

Sec.  7,  N.  W.  qr.,  -            -  -    233 

9,  N.  W.  qr.,        -  -            431 

11,  N.  E.  qr.,     -  -    219 

Forrest  House  station,  240 

Brookfield  June.,     -  -    246 

Elm  Grove  station,       -  170 

Burnett.    T.  12,  R.  15  E. 

Burnett  June.,        -  -    299 

Lake  Horicon,  277 

Burlington.    T.  2,  R.  19  E. 
Sec.  5,  N.  E.  qr.,    - 

Burlington  station,      -  206 
Sec.   4,  mid.  N.  line  N.  E.  qr.,      -     179 

5,  mid.  S.  line,    -  -            210 

6,  mid.  W.  line,         -  -    230 

7,  -  263 

8,  mid.  S.  line,  -    223 

17,  lake,    -  200 
Calamus.    T.  11,  R.  13  E. 

Sec.  6,  mid.  N.  line  N.  E.  qr.,      -    366 

7,  mid.  S.  M.,     -  361 
Loss  Lake,                          -  -    291 
Sec.  18,  center  N.  hi,  400 

18,  center,        -  •    394 

18,  near  center,     - 

19,  near  center  N.  line,  -    277 

19,  S.  W.  qr.,       -  276 
23,  N.  E.  qr.,  stream,  -    258 
27,  N.  E.  qr.,        -  -            305 
27,  center  E.  hf.,  swamp,        -    270 
31,  N.  W.  corner,  265 
31,  S.  W.  comer,  marsh,         -    239 

34,  N.  W.  qr.,      -  266 

35,  S.  W.  qr.,  -     297 
35,  S.  W.  qr.,  ridge,  -            318 

Caledonia.    T.  4,  R.  22  E. 
Sec.   5,  Root  river, 

5.  near  S.  line,    - 

8,  mid.  S.  line,  -     141 

17,  mid.  S.  line,    -  152 

20,  mid.  S.  line  S.  E.  qr.,        -     161 
Franksville  station, 

Sec.  31,  center,       -  -    169 

33,  S.  W.  qr.,  railroad,  -            111 

34,  E.  hf.,  -      90 

35,  E  hf.,  valley,  54 
T.  4,  R.  23,  E. 

Sec.  6,  S.  line,       -  -    110 

7,  S.  line,            -  -             80 

18,  S.  line,       -           -  -      70 

19,  center,             -  -             80 

20,  S.  line,       -           -  -      60 

27,  N.  E.  qr.,        -  18 
29,  S.  line,       -            -  -      60 

Calumet.    T.  17,  R.  19  E. 

Sec.  26,  mid.  N.  line,  -  381 

28,  near  W.  line,  stream,        -    335 
35,  N.  W.  qr.,      -  410 

Cato.    T.  19,  R.  22  E. 

Sec.   1,  near  mid.  E.  line,  -           215 

1,  center  Kettle  Range,  -    245 

1,  near  mid.  W.  line,  -            274 


Cato.    T.  1'J,  R.  22  E.  —  (con.)  Feet. 

Sec.  2,  near  mid.  W.  line,  -     255 

2,  mid.  N.  line  S.  E.  qr.,  280 
Cato  Corners,  hill,  -     301 
Sec.   3,  S.  W.  qr.,  stream.       - 

3,  near  mid.  W.  line,  -    246 

4,  near  mid.  W.  line,      -  288 

5,  near  mid.  W.  line,  -    263 
5,  S.  W.  qr.  of  N.  E.  qr.,  263 

5,  N.  W.  qr.  of  N.  E.  qr.,  -    277 

6,  S.  E.  qr.  top  of  quarry,  346 
6,  near  mid.  W.  line,  -    275 

27,  N.  E.  qr.LowerCato  Falls,     2-V> 

28,  Clark's  mills,  river,     -  159 

32,  mid.  E.  hf.,            -  -    277 
35,  N.  W.  corner,  269 
35,  center  N.  E.  qr.,  Kettles,  -     25'J 

Carlton.    T.  22,  R.  24  E. 

Sec.  6,  E.  Twin  river  -  80 

6,  S.  E.  qr.,  Michicott  river,  -      76 

20,  mid.  S.  line,    -  131 

28,  N.  E.  corner,  -      71 

31,  mid.  S,  line,  creek,      -  30 

33,  S.  line,  Michicott  river  -      24 
Casco.    T.  24,  R.  23  E. 

Casco  village    -  157 

Stream  E.  of  Casco,  -    128 

Sec.  7,  Cowles'  creek,  186 

9,            -           -           -  183 

13,  mid.  W.  hf.,  hill,  -  -    235 

14,  E.  line,  N.  E.  qr.,       -  95 
14,  near  middle,  -     165 
14,  S.  E.  corner,       -        -  123 
14,  S.  W.  qr.,  W.  side  hill,  230 

14,  S.  W.  qr.,  high  ridge,  -    252 

15,  S.  E.  qr.,  stream, 

16,  average  level,         -  -    220 

17,  level  of  upland  21'J 

Cedarbnrg.    T.  10,  R.  21  E. 

Sec.  4,  N.  E.  qr.  of  N.  W.  qr.,  -    296 

4,  mid  S.  line,  N.  W.  qr.,  :•,::•_' 

Mud  lake,  -    294 

Sec.   6,  S.  W.  corner,  -  352 

8,  N.  W.  corner  -     308 

Grafton  above  dam,     -  163 

Grafton  station,  -     170 

Sec.  26,  mid.  W.  hf.,   -  180 

26,  mid.  E.  line,  -    193 

a3,  mid.  E.  line    -  240 

33,  mid.  S.  line,  -    222 

Cedarburg  station         -            -  191 

Cedar  creek  at  R.  R.  bridge,  -    177 

Sec.  35,  center  W.  hf.,  168 

35,  N.  W.qr.,  -     167 

35,  S.  E.  qr.,  118 

Center.    T.  3,  R.  HE. 

Sec.   9,  stream  and  marsh,  -    293 

16,  N.  E.  qr.,        -  363 

16,  center,        -  -    364 

20,  N.  W.  qr.,       -  400 

21,  center  N.  W.  qr.,  -    389 

32,  N.  E.  qr.,        -  354 

33,  N.  W.  corner, 

Footville  station,  238 


TOPOGRAPHY. 


109 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Centerville.    T.  17,  R.  23  E. 

Sec.   3,  mid.  N.  line    - 
3,  creek, 

10,  near  mid.  N.  line, 

15,  N.  W.  corner, 

15,  Fish  creek, 

21,  N.  E.  comer, 

28,  N.  E.  corner, 

28,  center  E.  line, 

33,  N.  E.  corner,  - 
Charlestown.    T.  18,  R.  20  E. 
Chilton  station,  - 

Sec.  20,  Hayton  station, 
Hayton  village,  stream, 
Sec.  22,  E.  line  (est.), 
Chilton.    T.  18,  R.  19  E. 
Sec.  13,  general  level, 

26,  N.  W.  qr.  (est.), 

27,  mid.  N.  W.  qr.  (est.), 

28,  N.  E.  qr.  (est.),  stream 
Claybanks.    T.  26,  R.  26  E. 

Sec.  29,  N.  E.  qr.,  top  of  terrace, 

29,  N.  E.  qr.,  bottom  of  terrace, 
Clinton.    T.  1,  R.  14  E. 

Sec.   2,  E.  hf., 

2,  S.  W.  qr.,       - 
9.  center, 

10,  N.  W.  qr.,       - 

17,  Clinton  Junction,   - 

18,  N.  E.  qr., 
Clyman.    T.  10,  R.  15  E. 

Sec.   6,  N.  W.  qr.,  creek    - 
18,  mid.  E.  line,  marsh,  - 
20,  near  N.  W.  corner, 
20,  center,  N.  E.  qr.  of  N.  E.  qr 
28,  Clyman  station, 
Cold  Spring.    T.  5,  R.  15  E. 
Three-qr.  miles  S.  of  Hebron, 
Bark  river  marsh, 
Cold  Spring  village, 
Cold  Spring  mill  pond, 
Concord.    T.  7,  R.  16  E. 
Concord  village, 
Sec.  30, 

Cooperstown.    T.  21,  R.  22  E. 
Sec.    1,  S.  W.  qr.,       - 

11,  mid.  S.  line,  stream, 

23,  mid.  S.  line,    - 

24,  mid.  N.  hf., 

25,  N.  E.  qr.,  bottom  of  ledge, 
35,  mid.  S.  line,  outcrop, 

Dale.    T.  21,  R.  15E. 

Medina  station, 
Darien.    T.  2,  R.  15  E. 
Sec.  24,  S.  W.  qr.,  hill 
28,  S.  E.  qr., 
28,  Darien  station, 
31,  mid.  E.  line,    - 
31,  S.  W.  comer, 
33,  W.  line, 

Delafield.    T.  7,  R.  18  E. 
Lakeside  Station,    - 
Pine  Lake  Station, 
Nagowicka  Lake,    - 
Pewaukee,        ... 


Feet. 
64 
47 
63 
66 
30 
60 
67 
53 
61 


269 
249 
227 
242 

336 
398 
392 
669 

87 
12 

370 
352 
373 
362 
364 
338 

227 
231 

258 
277 
330 

296 
223 
226 
212 

287 
324 

219 
184 
240 
172 
69 
266 

192 

398 
363 
367 
290 
341 
290 

292 
350 
304 
263 


Delavan.    T.  2,  R.  16  E.  Feet. 

Sec.   2,  S.  E.  qr.,     -  -    383 

3,  S.  E.  corner,    -  -            385 

9,  S.  line,        -            -  -    375 

10,  W.  line,          -  390 

17,  E.  hf.,         -  -    356 

17,  Delavan  Station,  -            342 

19,  N.  W.  qr.,  -    327 

24,  hill,     ---  571 

De  Pere.    T.  33,  R.  21  E. 

Sec.  26,  center  N.  hf.,  -    245 

28,  ledge,  -  114 

33,  -           -           -  -    213 
Dover.    T.  3,  R,  20. 

Sec.  13,  mid  N.  line,            -  -    261 

17,  N.  W.  qr.,      -  253 

Eagle  Lake,            -  -    223 

Sec.  25,  S.  hf.,             -  -           263 

Kansasville  Station,            -  -    240 

Sec.  28,                        -  -           217 

Dover  Station,        ...    234 

Sec.  33,  N.  E.  qr.,        -  -            230 

Eagle.    T.  5,  R.  17  E. 

Sec.  12,  near  mid.  N.  line,  -  -    355 

14,  near  N.  E.  corner,  -            363 

14,  N.  E.  qr.,  -            -  -    370 

19,  S.  E.  qr.,         -  -            292 

19,  mid.  W.  line,         -  -    266 

20,  S.  E.  qr.,         -  -            324 

21,  E.  hf.,        -            -  -    355 

22,  mid.  W.  hf.,  Eagle,  -           365 
22,  N.  E.  qr.,  -            -  -    359 

East  Troy.    T.  4,  R,  18  E. 

Honey  Creek,  S.  of  village,  -    239 
Eaton.    T..18,  R.  21  E. 

Sec.  18,  S.  E.  qr.,    -  -    221 

19,  S.  E.  qr.,         -  -            295 

32,  N.  W.  qr.,              -  -    276 
Eden.    T.  14,  R.  18  E. 

Sec.   6,  N.  W.  corner,        -  -    433 

22,  center,  463 

22,  S.  line,        -            -  -    489 

24,  S.  W.  qr.,        -  472 

25,  N.  hf.,  creek,  -    404 
25,  N.  W.  qr.,      -  515 
27,  N.  E.  qr.,  river,      -  -    434 
27,  S.  E.  qr.,          -  -            432 
27.  N.  line  N.  E.  qr.,  -  -    415 

Egg  Harbor.    T.  29,  R.  26  E. 

1  mile  S.  of  Egg  Harbor,    -  -     180 

Sec.  22,  N.  W.  qr.,      -  -            154 

27,  N.  W.  corner,        -  -     172 

27,  W.  hf.,            -  150 

27,  S.  W.  qr.,  -  -     137 

34,  N.  W.  corner,  swamp,  139 
Egg  Harbor.    T.  30,  R.  27  E. 

Sec.  29,  N.  E.  qr.,       -  -     180 

Elba.    T.  10,  R.  13  E. 

Sec.   1,  mid.  S.  line,  -    249 

6,  S.  W.  comer,  Crawfish,  235 

Elba  R.  R.  crossing,  -    251 

Sec.  16,  N.  line  N.  E.  qr.,  -            294 

16,  S.  E.  qr.  R.  R.,      -  -    258 

Danville,  289 

Sec.  25,  S.  W.  qr.,              -  -    219 


110 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Elba.    T.  10,  R.  13  E.  —  (con.)  Feet. 

Sec.  27,  N.  E.  qr.,  Crawfish,    -  232 

28,  S.  W.  qr.,  -            -  -    257 

30,  Crawfish,                      -  251 

81,  N.  W.  qr.,             -  -    277 

Emmet.    T.  9,  R.  15  E. 

Sec.   5,  mid.  E.  line,  -    302 

20,  S.  E.  qr.,  quarry,        -  282 

32,  R,  R.,  -    243 
Rock  river  N.  of  Watertown,  -  211 

Empire.    T.  15,  R.  18  E. 

Sec.  4,  S.  E.  corner,    -           -  399 

12,  N.  W.  qr.,  lowland,  -    368 
Erin.    T.  9,  R.  18  E. 

Sec.    1,  S.  W.  qr.  of  S.  E.  qr.,  -    668 

1,  S.  E.  qr.,  hill,              -  674 

14,  S.  W.  corner,         -  -    517 

14,  Lapham's  peak,  824 
Farmington.    T.  7,  R.  15  E. 

Johnson's  Creek  station,     -  -     193 

Sec  28,  N.  E.  qr.,  260 
Farmington.    T.  12,  R.  20  E. 

Sec.   6,  S.  W.  qr.,  stream,  -    362 

6,  near  N.  W.  qr.,  439 

9,  near  N.  E.  corner,  -    254 

21,  N.  E.  corner,  -  230 
27,  mid.  S.  line,  -    315 
30,  W.  line,  411 

33,  N.  W.  corner,        -  -    277 
Forrest.    T.  15,  R.  19  E. 

Sec.   7,  E.  hf,  Sheboygan  river,  -    356 

9,  S.  W.  qr.,        -  410 

9,  S.  E.  corner,  stream,  -    360 

13,  center  N.  E.  qr.,  498 

13,  E.  line  N.  E.  qr.,   -  .  -    497 

14,  near  E.  line,   -  445 
14,  center,        -  -    428 

16,  N.  E.  qr.,        -            -  389 

24,  center  N.  hf.,  -    424 

25,  S.  W.  qr.,  stream,      -  451 
36,  center  N.  W.  qr.,  -  -    515 

Forrestville.    T.  26,  R.  25  E. 

Sec.  17,  mid.  E.  line  S.  W.  qr.,  170 

30,  N.  E.  qr.,  river,      -  3 
32,  mid.  E.  hne(?)  119 

Fox  Lake.    T.  13,  R.  13  E. 

Emily  Lake,  -    312 

Sec.  4,  mid.  N.  line,   -  377 

4,  mid.  S.  line,           -  -    346 

5,  mid.  N.  line,  -  382 
5,  N.  W.  qr.,              -  -    412 

17,  S.  E.  qr.,         -  293 

31,  N.  W.  qr.  of  N.  W.  qr.,  377 
31,  mid.  W.  line  N.  W.  qr.,  -    383 
31,  S.  W.  qr.,       -           -  381 

Franklin.    T.  5,  R.  21  E. 

Sec.  3,  N.  line  N.  E.  qr.,  -  -    153 

3,  angle,  Loomis  rd.,  E.  of  riv.,  133 

3,  Root  river,  Loomis  rd.,  -     118 

3,  W.  line  N.  E.  qr.,       -  130 

3,  W.  line  S.  W.  qr.,  -     190 

4,  N.  W.  corner,  130 

5,  N.  W.  corner,        -  -    205 

5,  N.  line,  angle  of  ru.,  -  230 

6,  N.  line,  on  rd.,      -  -    235 


Franklin.    T.  5,  R.  21  E.  —  (con.)    Feet. 

Franklin  Village  (hotel),  218 

Sec.   6,  E.  of  center,  on  rd.,    -  250 

7,  N.  line,       -  -    210 

7,  S.  line  N.  W.  qr.,  road,  -    220 

7,  N.  W.  qr..  brook,        -  183 

8,  near  N.  W.  cor.,  road,  -    200 
8,  N.  line,  R.  R.  grade,  -  183 
8,  W.  line  S.  W.  qr.,  road,  -     226 
8,  center  S.  W.  qr.,         -  215 
8,  mid.  W.  line  S.  E.  qr.,  -     199 
8,  N.  W.  qr.,  angle  of  roads,     198 

8,  Lake,    '  -    172 

9,  mid.  N.  line  N.  E.  qr.,  206 
9,  mid.  N.  line,  -     212 
9,  mid.  N.  line  N.  W.  qr.,  215 
9,  N.  W.  corner,        -  -     194 
9,  N.  line  S.  W.  qr.,       -  212 
9,  center  S.  W.  qr.,    -  -    216 
9,  mid.  W.  line  N.  E.  qr.,  217 

10,  mid.  N.  line  N.  E.  qr.,  -     120 

10,  N.  line,  Root  river       -  113 

10,  mid.  N.  line,          -  -     134 

10,  mid.  N.  line  N.  W.  qr.,  155 

10,  N.  W.  corner,        -  -     180 

10,  mid.  W.  line  N.  W.  qr.,  173 

10,  mid.  W.  line,         -  -    185 

10,  mid.  W.  line  S.  W.  qr.,  190 

11,  mid.  N.  line  N.  E.  qr.,  -    155 
11,  mid.  N.  line,  -  140 
11,  mid.  N.  line  N.  W.  qr.,  -     125 

11,  N.  W.  corner,  125 

12,  mid.  N.  line  N.  E.  qr.,  -    183 
12,  mid.  N.  line,  -           -  158 
12,  mid.  N.  line  N.  W.  qr.,  -    180 
12,  mid.  N.  line  W.  hf.  N.W.  qr.,  190 

12,  N.  W.  corner,        -  -     178 

13,  mid.  N.  line  N.  E.  qr.,  138 
13,  mid.  N.  line,  -     138 
13,  mid.  N.  line  N.  W.  qr.,  158 

13,  N.  W.  corner,        -  -     147 

14,  mid.  N.  line  N.  E.  qr.,  137 
14,  mid.  N.  line,          -  -     1:5') 
14,  mid.  N.  line  N.  W.  qr.,  154 
14,  mid.  N.  line  W.  hf.  N.W.  qr.,  165 

14,  N.  W.  corner,  138 

15,  N.  line,  Root  river,  -     105 
15,  mid.  N.  line,  -  157 
15,  mid.  N.  line  N.  W.  qr.,  -     182 
15,  mid.  N.  line  W.  hf.  N.W.  qr..  141 
15,  N.  W.  corner,        -  -     167 
15,  mid.  W.  line,  185 

15,  mid.  W.  line  S.  W.  qr.,  -    200 

16,  mid.  N.  line  N.  E.  qr.,  188 
16,  mid.  N.  line,  -    176 
16,  mid.  N.  line  N.  W.  qr.,  175 

16,  N.  W.  corner,        -  -     197 

17,  mid.  N.  line,   -  200 
17,  jet.  Loomis  &  Franklin  rds.,  215 

17,  S.  line  N.  E.  qr.,        -  210 

18,  N.  line,  R.  R.  grade,  -    215 
18,  N.  W.  comer,  223 
18,  W.  line  N.  W.  qr.  R.  R.,  -    205 
20,  N.  line,  Loomis  road,  220 
20,  W.  line,  Loomis  road,  -    206 


TOPOGRAPHY. 


m 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 

Franklin.    T.  5,  R.  21  E.  —  (con.) 
Sec,  22,  mid.  W.  line  S.  W.  qr., 
22,  N.  W.  corner, 
22,  W.  line  near  N.  W.  cor., 
22,  mid.  W.  line  N.  W.  qr., 
22,  mid.  W.  line, 
25,  mid.  N.  line  N.  E.  qr., 
25,  mid.  N.  line,  - 
25,  mid.  N.  line  N.  W.  qr., 

25,  N.  W.  corner, 

26,  mid.  N.  line  N.  E.  qr., 
26,  mid.  N.  line,   - 

26,  mid.  N.  line  N.  W.  qr., 

26,  N.  W.  comer, 

27,  N.  line,  Root  river, 
27,  mid.  N.  line,  - 

27,  mid.  N.  line  N.  W.  qr., 
27,  N.  W.  corner, 
27,  mid.  W.  line  N.  W.  qr., 
27,  mid.  W.  line, 

27,  mid.  W.  line  S.  W.  qr., 

28,  N.  W.  corner, 

29,  mid.  W.  line  N.  W.  qr., 

29,  N.  W.  corner, 

30,  mid.  N.  line  N.  E.  qr., 

30,  mid.  N.  b'ne,  - 

34,  mid.  N.  line  N.  E.  qr., 
34,  N.  line,  Root  river, 
34,  mid.  N.  line, 

34,  N.  W.  corner, 

35,  mid.  N.  line  N.  E.  qr., 
35,  mid.  N.  line,  - 

35,  mid.  N.  line  N.  W.  qr., 

35,  N.  W.  corner, 

36,  mid.  N.  line  N.  E.  qr., 
36,  mid.  N.  line,  - 

36,  mid.  N.  line  N.  W.  qr., 
36,  N.  W.  corner, 
Franklin.    T.  20,  R.  22  E. 
Sec.   1,  S.  W.  corner, 

1,  S.  W.  qr.,       - 

2,  highest  pt.  of  Kettle  range, 
4,  S.  W.  qr.,  - 

19,  mid.  W .  line, 

31,  S.  E.  corner, 

31,  mid.  S.  line,  high  ridge, 
Franklin.    T.  22,  R.  23  E. 
Sec.  11,  N.W.  qr., 

15,  center  N.  E.  qr., 
22,  S.  line  S.  E.  qr.,     - 
34,  N.  W.  comer,  creek,  - 
34,  S.  W.  corner, 

34,  S.  E.  qr.,  creek, 
Fredonia.    T.  12,  R.  21  E. 

Sec.    1,  N.  E.  corner, 
12,  S.  E.  corner,    - 
22,       - 
25,  S.  E.  corner    - 

28,  Waubakee  village, 

29,  Quarry  on  N.  side  river, 
33,  Milwaukee  River, 

35,  S.  Iin9  S.  W.  qr.,  R.  R., 
Predonia  Station,    - 

Fulton.    T.  4,  R.  12  E. 
Newville  Bridge,     - 


Feet. 

Fulton.    T.  4,  R.  12  E.  —(con.) 

Feet. 

182 

Edgerton  Station, 

242 

175 

Sec.   3,  center  N.  line, 

-      251 

170 

4,  center  N.  hf., 

232 

175 

5,  center  S.  line, 

-    273 

168 

5,  S.  line  S.  E.  qr., 

284 

132 

6,  N.  W.  qr., 

-    240 

153 

10,  S.  W.  qr.,       - 

219 

132 

Geneva.    T.  2,  R.  17  E. 

163 

Sec.   2,  S.  E.  qr., 

436 

190 

5,  S.  hf., 

-    445 

157 

6,  mid.  E.line,    - 

415 

138 

6,  Elkhorn  Station,     - 

-    415 

130 

9,  center  E.  hf.,   - 

402 

96 

9,  mid.  E.  line,  R.  R., 

-    406 

110 
112 

9,  N.  W.  qr.,       - 
10,  mid.  E.  line, 

418 
-    400 

146 

10,  near  center,    - 

423 

122 

10,  W.  hf.,      - 

-    415 

103 

13,  N.  W.  corner, 

337 

114 

14,  near  center, 

-    342 

190 

23,  S.  hf., 

277 

190 

25,  W.  line,    - 

-    333 

195 

34,  mid.  E.  line, 

-    345 

196 

36,  Geneva  Station, 

300 

218 

Lake  Geneva, 

282 

100 

Genesee.    T.  6,  R.  18  E. 

92 

Genesee  Station, 

325 

106 

Saysville  Mill  Pond,    - 

232 

105 

Sec.  13,  N.  line,      - 

-    327 

148 

14,  S.W.qr., 

.     313 

126 

15,  mid.  S.  line, 

-    329 

110 

21,  N.  E.  qr.,  creek,     - 

-    315 

100 

21,  mid.  S.  line,     - 

331 

158 

21,  hill, 

-    350 

140 

25,  mid.  N.  E.  qr., 

228 

118 

25,  center  S.  W.  qr.,    - 

-     2J5 

130 

29,  S.  E.  corner,    - 

359 

31,  North  Prairie  Station 

-    363 

277 

35,  mid.  S.  line  N.  W.  qr., 

367 

335 

Germantown.    T.  9,  R.  20  E. 

303 

Sec.  5,  N.  line,  R.  R., 

278 

300 

6,  N.  E.  qr.,   - 

-    289 

311 

9,  N.  Line,  R.  R., 

313 

297 

10,  N.  W.  corner, 

-    276 

320 

10,  center  S.  hf., 

297 

15,  S.  E.  qr.,  Menomonee  River,  273 

168 

16,  W.  line,  R.  R., 

298 

286 

17,  mid.  line,  R.  R.,     - 

-    318 

112 

17,  W.  line,  R.  R., 

328 

90 

18,  W.  line,  R.  R.,      - 

-    360 

92 

21,  N.  line,  R.  R., 

286 

62 

22,  W.  line,  R.  R.,     <• 

-    273 

22,  center, 

275 

279 

23,  N.  W.  qr.,  R.  R..  - 

-    301 

202 

23,  W.  line,  R.  R., 

295 

303 

23,  mid.  S.  line.  R.  R., 

-    203 

229 

25,  S.  line,  R.  R., 

248 

194 

25,  W.  line,  R.  R.,      - 

-    278 

197 
169 

26,  S.  E.  qr., 
28,  mid.  N.  line, 

313 
-    286 

228 

30,  mid.  E.  line,  S.  E.  qr., 

276 

206 

32,  N.  W.  corner, 

-    296 

32,  center, 

284 

208 

35,  S.  W.  corner, 

-    319 

112 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OF  ELEVATIONS  ABOVE  LALE  MICHIGAN  —  continued. 


Germantown.  T.  9,  R.  20  E.  —(con.)  Feet, 

Sec.  35,  center  S.  W.  qr.,        -  195 

35,  near  S.  W.  corner,  -    314 

35,  mid.  S.  line  S.  W.  qr.,  270 

36,  S.  line,  R.  R.,        -  -     198 
36,  S.  E.  corner,  R.  R.,     -  193 
36,  center  S.  W.  qr.,   -  -     195 

Gibson.    T.  21,  R.  23  E. 

Sec.    1,  N.  line  N.  E.  qr.,  -  -      63 

7,  mid.  N.  hf.,    -  96 
9,  N.  E.  qr.,  -     160 

21,  near  S.  W.  comer,      -  174 

24,  E.  line  S.  E.  qr.,    -  -      83 
26,  S.  W.  qr.,  Jambo  Creek,  49 

Gillette.    T.  28,  R.  19  E. 

Sec.   1,  Little  River,    -  164 

25,  Oconto  River  above  the  falls,  132 
Grafton.    T.  10,  R.  22  E. 

Sec.  5,  mid.  N  hf.,  -    174 

8,  S.iine,R.  R.,  -  117 

9,  near  center S.hf.,  -  -     111 

19,  N.  E.  qr.  of  N.  W.  qr.,  211 

20,  mid.  N.  hf.,  R.  R.,  -    119 
20,  mid.  E  line  N.  E.  qr.,  150 
20,  bank  Lake  Michigan,  -     119 
20,  S.  line,  R.  R.,  130 
29,  S.  line,  R.  R.,        -  -      96 
32,  S.  line,  R.  R.,  97 

Granville.    T.  8,  R.  21  E. 

Sec.    1,  mid.  N.  line,                -  68 

1,  N.  line,  river  -      56 

2,  N.  line,  Cedarburg  P.  Road,    68 
2,  mid.  N.  line,  R.  R.,  -      83 
2,  N.  W.  corner,  89 

2,  S.  E.  qr.  brook      -  -      74 

3,  mid.  N.  line,  75 

3,  N.  W.  corner,        -  -      87 

4,  mid.  N.  line,     -            -  100 

4,  N.  W.  corner, 

5,  N.  W.  corner,  145 

6,  mid.  N.  line,          -  -     190 
6,  W.  line,  C.,M.  &  St.  P.  R.  R.  190 
6,  mid.  W.  line,        -  -     173 

6,  N.  line  S.  W.  qr.  R.  R.  186 

7,  N.  hne  R.  R.         -  -    169 
7.  mid.  N.  line,    -  206 

7,  N.  W.  corner,        -  -     169 

8,  mid.  N.  line,    -  165 
8,  W.  line,  Granville,       -  167 

8,  mid.  W.  line,  -    184 

9,  mid.  N.  line,    -  125 
9,  N.  W.  corner,       -  -    179 

10,  mid.  N.  line,    -  84 

10,  mid.  N.  line,  N.  W.  qr.  122 

10,  N.  W.  corner,  98 

10,  Whittaker's  house,  -    103 

11,  N.  hne  R.  R.  -           -  85 
11,  mid.  N.  line,  -      79 

11,  N.  W.  corner,  77 

12,  N.  line  river,  -      54 

12,  N.  W.  corner,  89 

13,  N.  W.  corner,        -  -     123 

13,  mid.  W.  line,  166 

14,  mid.  N.  line,  -      99 
14,  N.  W.  corner,             -  119 


Granville.    T.  8,  R  21  E.  —  (con.)  Feet. 

Sec.  15,  N.  line  R.  R.,        -  -     158 

15,  N.  W.  corner,  185 

16,  mid.  N.  line,  -     177 

16,  N.  W.  corner,               -  175 

17,  N.  line  R.  R.,       -  -     142 
17,  mid.  N.  line,                -  167 
17,  N.  W.  corner,        -  -    213 
19,  mid.  N.  Hne,  N.  E.  qr.,  168 
19,  mid.  N.  line,         -  -    180 
19,  mid.  W.  hne,  N.  E.  qr.,  212 

19,  center,       -  -     190 

20,  N.  E.  comer, water  in  E.  br.,  124 
20,  mid.  N.  line,  N.  E.  qr.,  160 
20,  mid.  N.  hne,  -     152 

20,  N.  W.  corner,  215 

21,  N.  hne,  M.  &  St.  P.  R.  R.     168 
21,  mid.  N.  line,    -  188 

21,  N.W.  corner,        -  -    136 

22,  mid.  N.  hne,    -           -  180 
22,  N.  W.  corner,        -  -     160 

22,  center  R.  R.,  154 

23,  mid.  N.  line,  -    115 
23,  mid.  N.  line  N.  W.  qr.,  145 

23,  N.  W.  corner,       -  -     135 

24,  mid.  N.  line  E.  qr.  N.  E.  qr.  135 
24,  mid.  N.  hne,  N.  E.  qr..  98 
24,  N.  line  W.  C.  R.  R.,  -    112 
24,  N.  W.  corner,  131 
24,  W.  hne  R.  R.,      -  -     138 
24,  N.  hne  S.  E.  qr.  R.  R.,  115 

24,  mid.  W.  line  S.  W.  qr.,  150 

25,  N.  W.  corner,  109 
25,  N.  hne  R.  R.,        -  -      93 
25,  mid.  W.  line,  105 
25,  N.  line,       -  -     129 
25,  N.  line  N.  W.  R.  R.,  115 
25,  mid.  N.hne,     -  111 

25,  mid.  N.  line  N.  W.  qr.,  102 

26,  mid.  N.  hne  N.  E.  qr.,  129 
26,  mid.  N.  hne,    -  110 

26,  W.  hne  S.  E.  qr.  R.  R.,  107 

27,  N.  W.  corner,  130 
27,  mid.  N.  line  N.  E.  qr.,  135 
27,  mid.N.hneW.hf.N.E.qr.  179 
27,  mid.  N.  hne,  -     154 

27,  N.  W.  corner,  148 

28,  mid.  N.  line,  N.  E.  qr.,  177 
28,  mid.  N.  line,    -  147 

28,  N.  W.  corner,        -  -     161 

29,  200  ft.  W.  N.  E.  corner,  175 
29,  N.  hne,  N.  F.  du  Lac  R'd,    121 
29,  mid.  N.  line,  138 

29,  N.  W.  corner,  152 

30,  mid.  N.  hne,          -  -    218 
30,  mid.  N.  hne  N.  W.  qr.,  170 
30,  N.W. corner,        -  -     145 

30,  center,  170 

31,  N.  hne,  E.  branch,  -     118 
31.  mid.  N.  line,  150 
31,  mid.  N.  line  N.  E.  qr.,  130 
31,  N.  W.  corner,  158 
31,  center,        -  -     160 

31,  mid.  W.  hne  S.  E.  qr.,  125 

32,  mid.  N.  hne,    -  162 


TOPOGRAPHY. 


113 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Granville.    T.  8,  R.  21  E.  — (con.)    Feet. 

Sec.  33,  mid.  N.  line,  -    134 

33,  mid.  W.  line,  160 

33,  center  N.  E.  qr.,    -  -     154 

34,  mid.  N.  line  N.  E.  qr.,  106 
34,  mid.  N.  line,         -  -    136 
34,  N.  W.  corner,  160 

34,  mid.  W.  line,        -  -     140 

35,  N.  line  R.  R.,  94 
35,  mid.  N.  line,         -  -      97 

35,  N.  W.  comer,  •  97 

36,  N.  line  W.  C.  R.  R.,  -      56 
36,  N.  W.  corner,  96 
36,  W.  line  R.  R.,      -  -      93 
36,  mid.  N.  line  W.  hf.  S.  W.  qr.  94 
36,  mid.  N.  line  S.  E.  qr.  R.  R.,    58 
36,  S.  E.  qr..  Schwartzburg  St'n,  66 

Green  Bay.    T.  24,  R.  22  E 

Sec.  13.  mid.  S.  line,  -    238 

13,  Outcrop,           -            -  80 

22,  W.  hf.,nearFranken,  219 

T.  25,  R.  22  E. 

Whitney's  Bluff,  91 

Sec.  16,  On  bluff,    -           -  -    100 

Greenbush.    T.  15,  R.  20  E. 

Glenbulah  Station,             -  -    289 

Sec.-4,  center,              -           -  466 

St.  Cloud  Station,               -  -    349 

Sec.   6,  N.  E.  comer,  323 

8,        -           -           -  -    416 

10,  center,             -           -  289 

35,  mid.  W.  line,  plateau,  408 

36,  center  summit  of  ridge,  -    524 
36,  near  center,  road,       -  513 

Greenbush  hotel,                -  -    297 

stream,     -  283 

Hill  S.  of  Greenbush,         -  -    417 

Greenfield.    T.  6,  R.  21  E. 

Sec.    1,  mid.  W.  line,  -      62 

2,  W.  line  N.  W.  qr.,     -  82 

2,  mid.  W.  line,         -  -      94 

3,  W.  line,                      -  156 
3,  N.  of  center,  creek,  -    124 

3,  N.  line,  Muckwonago  road,   132 

4,  mid.  N.  line,  -     125 
4,  N.  W.  corner,             -  180 
4,  near  center,  Poplar  creek,       136 
4,  center,  143 
4,  center  S.  W.  qr.,    -  -     158 

4,  W.  line,                       -  173 

5,  mid.  N.  line,          -  -    219 

5,  N.  W.  corner,             -  155 

6,  mid.  N.  line,          -  -    154 
6,  N.  W.  corner,             -  178 
6,  mid.  W.  line  N.  W.  qr.,  -     190 

6,  mid.  W.  line,  205 

7,  N.  W.  corner.        -  -     174 
7,  near  N.  W.  cor.,  Root  river,  169 
7,  mid.  W.  line  N.  W.  qr.,  -     189 
7,  mid.  W.  line,              -  178 
7,  mid.  W.  line  S.  W.  qr.,  -     178 

7,  mid.  line  S.  E.  qr.,     -  199 

8,  N.  line,  Muckwonago  road,  212 
8,  mid.  W.  line  N.  E.  qr.,  -    170 
8,  N.  line  S.  E.  qr.,        -  151 

Wis.  Sun.— 8 


Greenfield.    T.  5,  R.  21  E.  —  (con.)  Feet. 
Sec.  8,  W.  line  S.  E.qr.  Muckw'go  R.,  170 

8,  center  N.  W.  qr.,       "  173 

9,  N.  W.  corner,        -            -  200 
9,  N.  line  S.  E.  qr.,        -  141 

10,  mid.  N.  line,                       -  135 

11,  N.  line  N.  E.  qr.  R.  R.,  '90 
11,  N.  W.  corner,        -            -  112 
11,  mid.  W.  line  N.  W.  qr.,  127 
11,  mid.  W.  Ime,                     -  102 

11,  mid.  W.  line  S.  W.  qr.,  125 

12,  center,        -                        -  84 

12,  S.  W.  qr.,  Janesville road,  54 

13,  mid.  N.  line  N.  E.  qr.,      -  55 
13,  mid.  N.  line,  90 
13,  mid.  N.  line  N.  W.  qr.,     -  106 
13,  mid.  W.  line  N.  W.  qr.,  93 
13,  N.  W.  corner,        -           -  124 
13,  mid.  W.  line,  119 
13,  mid.  W.  line  S.  W.  qr.,    -  146 

13,  S.  line,  Loomis  road,  -  137 

14,  mid.  N.  line  N.  E.  qr.,      -  137 
14,  mid.  N.  line,  -           -  158 
14,  mid.  N.  line  N.  W.  qr.,     -  170 
14,  N.  line  R.  R.  grade,    -  146 
14,  N.  W.  corner,        -            -  140 
14,  mid.  W.  line,              -  192 
14,  W.line  S.W.qr., Janesville  R.  202 
14,  N.  E.  qr.,  Janesville  road,  177 

14,  S.  W.  qr.,  Janesville  road,  163 

15,  mid.  N.  line  N.  E.  qr.,      -  170 
15,  mid.  N.  line  W.  hf .  N.  E.  qr.,  183 
15,  mid.  N.  line,               -  175 
15,  mid.  N,  line  N.  "W".  qr.,     -  150 
15,  N.  W.  corner,  145 

15,  N.  line  N.  W.  qr.,  Brook,  140 

16,  mid.  N.  line  N.  E.  qr.,      -  155 
16,  mid.  N.  line,              -  170 
16,  mid.  N.  line  N.  W.  qr.,     -  200 
16,  W.  line,  Beloit  road,  -  225 
16,  mid.  W.  line  S.  W.  qr.,     -  183 
16,  mid.  W.  line  S.  E.  qr.,  215 
16,  center,        -                        -  209 

16,  mid.  W.  line  N.  E.  qr.,  183 

17,  mid.  N.  line  N.  E.qr.,      -  210 
17,  center,  200 
17,  S.  W.  qr.,  angle  Beloit  roacl,  190 

17,  W.  line,  Beloit  road,         -  180 

18,  N.  line,  Root  river,     -  149 
18,  mid.  N.  line  E.  hf .  N.W.  qr.,  156 
18,  mid.  N.  line  N.  W.  qr.,     -  161 
18,  N.  W.  comer,             -  193 
18,  mid.  W.  line  N.  W.  qr.,   -  212 
18,  mid.  W.  line,  182 
18,  mid.  W.  line  S.  W.  qr.,     -  212 

18,  mid.  W.  line  S.  hf.  S. W.  qr.,  236 

19,  N.  line,  Root  river,             -  145 
19,  mid.  N.  line  N.  E.  qr.,  170 
19,  mid.  N.  line,                       -  2:30 
19,  mid.  N.  line  N,  W.  qr.,  210 
19,  N.  W.  corner,        -            -  214 
19,  mid.  W.  line  N.  W.  qr.,  244 
19,  mid.  W.  line,         -            -  255 

19,  W.  line  S.W.  qr.,  Beloit  road,  245 

20,  mid.  N.  line  S.  E.  qr.,       -  178 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Greenfield.    T.  6,  E.  21  E.  —  (con.)  Feet. 

Sec.  20,  center,  159 

20,  mid.  line,  Root  river,        -  143 

21,  mid.  N.  Hue  N.  E.  qr.,  217 
21,  mid.  N.  line,          -            -  221 
21,  N.  W.  corner,             -  180 
21,  mid.  W.  line,         -            -  180 
21,  mid.  N.  line  S.  W.  qr.,  210 

21,  center,        -                       -  240 

22,  mid.  N.  line  N.  E.  qr.,  174 
22,  N.  line  N.E.  qr.,  R.R.  bridge,  172 
22,  mid.  N.  line,  185 
22,  mid.  N.  line  N.  W.  qr.,  199 
22,  N.  W.  corner,        -            -  188 
22,  mid.  W.  line,  220 
22,  W.  line,  Janesville  road,    -  244 
22,  center  S.  W.  qr.,  R.  R.,  240 

22,  N.  line  S.W.qr.,  Janesville  R.,  200 

23,  mid.  N.  line  N.  E.  qr.,      -  179 
23,  mid.  N.  line,  -            -  165 
23,  mid.  N.  line  N.  W.  qr.,     -  181 
23,  N.  W.  corner,  192 
23,  mid.  W.  line  N.  W.  qr.,    -  187 
23,  mid.  W.  line,              -  180 

23,  mid.  W.  line  S.  W.  qr.,     -  196 

24,  N.  line,  Loomis  road,  137 
24,  N.  W.  comer,        -            -  137 
24,  mid.  W.  line  S.  W.  qr.,  170 
24,  N.  line,  S.  W.  qr.,              -  122 
24,  W.  line,  N.  E.  qr.,  Loomis' 

Road,      -                        -  117 

26,  N.  line,  Loomis'  Road,  180 

26,  N.  W.  comer,        -            -  193 
26,  mid.  W.line,N.hf.N.W.qr..232 

26,  mid.  W.  line,  N.  W.  qr.,  -  220 

26,  mid.  W.  line,  227 

26,  mid.  W.  line,  S.  W.  qr.,    -  223 

26,  center  S.  W.  qr.,  210 

26,  center,        -                        -  186 

26,  N.  E.  qr.,  brook,        -  160 

27,  N.  W.  qr.,  R.  R.  grade,  195 

28,  N.  line  N.  E.  qr.,    Janes- 

ville Road,  -  198 

28,  N.  W.  comer,        -           -  157 

28,  W.  line  S.  W.  qr.,  RootR.,  141 

29,  S.E.  qr.,  Janesville  road,  -  199 

30,  N.  W.  corner,  265 
30,  mid.  W.  line  N.  W.  qr.,    -  254 
30,  mid.  W.  line                     -  234 

30,  mid.  W.  line  S.  W.  qr.,  229 

31,  N.  W.  corner,        -            -  223 
81,  center  W.  hf.  N.  W.  qr.,  233 
31,  N.  line  S.  W.  qr.,  road     -  212 
31,  center  brook,   -  192 

31,  mid.  N.  hf.  S.  E.  qr.,        -  192 

32,  N.  line  N.  E.  qr.,  Janesville 

road,       -                        -  224 

32,  Halo's  Corners,  211 

32,  n.id.  W.  line  S.  W.  qr. ,      -  195 

33,  N.  line  N.  E.  qr.,  Root  R.  128 
33,  mid.  N.  line,  R.  R.,           -  133 
33,  mid.  N.  line  N.  W.  qr.,     -  157 

33,  N.  W.  corner,  171 

34,  mid.  N.  line  N.  E.  qr.        -  152 
34,  mid.  N.  line,  -                     '  192 


Greenfield.    T.  6,  R.  21  E.  —  (con.)  Feet. 

Sec.  34,  mid.  N.  line  N.  W.  qr.,  -     180 

34,  N.  W.  corner,  156 

34,  near  S.  line,  Loomis  road,      153 

35,  N.  line,  Loomis  road,  -  198 
35,  N.  W.  comer,  -     202 
35,  mid.  W.  line  N.  W.  qr.,  152 
35,  N.  W.  qr.,  pond,  -     127 

Harmony.    T.  3,  R.  13  E. 

Sec.  2,  N.W.  qr.,    -            -  -    344 

Hartford.    T.  10,  R.  18  E. 

Hartford  Station,     -  -    408 

Sec.    1,  near  N.  "W.  corner,     -  487 

13,  near  S.  E.  corner,  stream,  411 

13,  center,  R.  R.,  453 

13,  W.  line,  R.  R.,      -  -    440 

14,  center,  R.  R.,  -            -  430 
14,  W.  line,  R.  R.,      -  -    430 
16,  N.  E.  corner,  466 

16,  center   E.  hf.,        -  -    403 

17,  W.  line,  R.  R.,           -  388 

18,  center,  R.  R.,         -  -    385 
18,  W.  line,  R.  R,,           -  392 
21,  center,  R.R.,  -           -  414 

21,  W.  line,  R.  R.,      -  -    406 

22,  center,  R.  R.,  -            -  428 
22,  W.  line,  R.  R.,      -  -    422 

24,  little  W.  of  mid.  of  E.  line,    740 

25,  -            -           -  -    566 
Hartland.    T.  26,  R.  17  E. 

Sec.  21,  Hartland,  -  -  257 
Hebron.  T.  6,  R.  15  E. 

Cushman's  mill  pond,  -  -  244 
Herman.  T.  16,  R.  22  E. 

Sec.  11,  N.  E.  corner,             -  235 

12,  mid.  N.  line,  N.  E.  qr.,  -     128 

13,  mid.  S.  line,    -  121 

26,  near  S.  line,  stream,  -     105 
26,  S.  E.  qr.,  stream,        -  147 

Holland.    T.  13,  R.  22  E. 

Sec.    1,  N.  line  R.  R.,        -  -      97 

12,  N.  line  R.  R.,  109 

13,  N.  line  R.  R.,        -  -    102 
16,  S.  E.  qr.,  bridge,        -  133 

24,  N.  line  R.  R.,        -  -    107 

25,  N.  line  R.  R.,             -  103 

26,  Cedar  Grove,          -  -     114 
29,  W.  line  N.  W.  qr.,     -  307 

35,  N.  line  R.  R.,         -  -    144 

36,  center  E.  line,  48 
Top  of  terrace  above  Amsterdam,  R. 

23,  -      47 
Bottom   of    terrace  above  Amster- 
dam, R.  47,  £ 
Holland.    T.  21,  R.  20  E. 
Sec.  20,  S.  E.  qr.,     -           -  -    233 
20,  S.  W.  qr.,        -  279 
Jackson.    T.  10,  R.  20  E. 
Sec.    1,  30  rods  W.  of  S.  E.  corner,    288 
1,  mid.  S.  line,  creek,  -    282 
1,  valley  of  creek,  292 
4,  mid.  S.  line  S.  E.  qr.,  -    292 
6,  center,  R.  R.,  -  386 

6,  N.  line,  R.  R.,       -  -    379 

7,  N.  E.  qr.,        -            -  440 


TOPOGRAPHY. 


115 


LIST  OP  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Jackson.    T.  10,  R.  20  E.  —  (con.)    Feet. 
Sec.  7,  mid   S.  line  S.W.  qr.,  valley,  396 

30,  N.  E.  qr.,  Cedar  creek,  •    275 

31,  mid.  S.  line,    -  319 

32,  S.  E.  qr.,  brook,     -  -    273 
:W,  N.  W.  corner,  R.  R.,  -  276 

32,  mid.  N.  line  N.  W.  qr.,  -    327 

33,  raid.  N.  line  N.  E.  qr.,  340 

34,  N.  W.  corner,        -  -    300 
34,  S.  W.  corner,  273 
36,  S.  E.  qr.,    -  -    208 
36,  S.  W.  qr.,       -  334 

Jacksonport.    T.  29,  R.  27  E. 
Ridge  S.  of  Jacksonport,     - 

Racine  Limestone,  58 
Coral  beds  hf .  mile  S.  of  Jacksonport,     20 

Sec.  33,  S.  hf.    -                        -  62 

Janesville.    T.  3,  R.  12  E. 

Janesville  Fair  Grounds,     -  -     295 

Janesville  Station,  240 

Jefferson.    T.  6,  R.  14  E. 

Jefferson  station,                        -  221 

Rock  river  at  Jefferson,       -  -     206 

Mouth  of  Crawfish  river,  200 

Sec.    9,  S.  E.  qr.,  stream,  -  -    242 

12,  N.  E.  qr.,  kill,  -  365 

15,  near  center  W.  hf.,  stream,    227 

17,  N.  E.  qr.,  269 

17,  N.  W.qr.,  quarry,  -  -    260 

18,  center  W.  hf.,  hill,       -  442 

19,  near  N.  W.  corner,  -    315 
Johnstown.    T.  3,  R.  14  E. 

Level  of  Rock  Prairie,        -  -    316 
Kewaskum.    T.  12,  R.  19  E. 

Sec.   5,  N.  line,  R.  R.,       -  -    398 

12,  mid.  E.  line,     -            -  409 

20,  mid.  E.  line,  stream,  -    410 
22,  S.  W.  qr.,  R.  R.,  354 
22,  mid.  N.  line,  -    409 
28,  near  mid.  N.  line,        -  528 
30.  N.  W.  corner,        -  -    463 

33,  N.  E.  corner,     -            .  362 

34,  N.  E.  qr.,  R.  R.,    -  -    363 

35,  R.  R.,  -  370 
Kewaunee.    T.  23,  R.  24  E. 

Sec.  5,  N.  W.  qr.,  ledge,  -  145 
14,  Kewaunee  river  at  bridge,  .  9 
14,  S.  W.  qr.,  junction  of  Lppcr 

Coral  and  Racine,      -  32 

20,  mid.  N.  line,  -    124 

26,  Est.,  general  level,       -  124 

30,  mid.  S.  line  -    138 

31,  outcrop,  140 
31,  N.  E.  qr.,  -  -    134 

Koshkonong.    T.  5,  R.  14  E. 

Fort  Atkinson  station,        -  -    249 

Marsh  below  Fort  Atkinson,     -  200 
Lake  Koshkonong,             -        (200)  184 

Kump's  quarry,  267 

Sec.  23,  center  W.  hf.,        -  -    257 

27,  S.  W.  qr.,         -  252 

31,  N.  E.  qr.,  quarry,  -  -    248 
34,  N.  E.  qr.,                      -  298 

32,  center  N.  hf.,  valley,  -    252 


Kossnth.    T.  20,  R.  23  E.  Feet. 

Sec.  12,  E.  line,  S.  E.  qr.,  river,     -  28 

15,  N.  E.  qr.,  124 

26,  S.  E.  corner,                       -  109 

36,  S.  E.  qr.,           -            -  93 

La  Fayette.    T.  3,  R.  17  E. 

Sec.    8,  near  center,  stream,           -  277 

18,  N.  E.  qr.,                      -  317 

19,  N.  E.  qr.,  -                        -  365 

30,  N.  E.  qr.,  437 

31,  N.  E.  qr.,   -                        -  44o 
31,  S.  W.  qr.,                      -  4138 

La  Grange.    T.  4,  R.  16  E. 

Sec.  1,  nearly  S.  of  hill,      -            -  365 

Heart  Prairie,    -                      .-  387 

Lake.    T..  6,  R.  22  E. 

Sec.    7,  mid.  N.  line,    -  60 

7,  mid.  N.  line,  N.  W.  qr.,    -  79 

7,  mid.  W.  line,   -  78 

7,  mid.  W.  line,  S.  W.  qr.,   -  50 

7,  mid.  N.  line,  S.  W.  qr.,  87 

7,  W.  of  center,                      -  64 

7,  N.  of  center,     -  80 

7,  center,  N.  E.  qr.,  -  65 

7,  highest  land  in  cemetery,  95 

8,  N.  E.  corner,                      -  17 
8,  mid.  S.  line,  S.  E.  qr.,  53 
8,  N.  W.  corner,        -            -  52 
8,  mid.  N.  W.  line,  N.  W.  qr.,  58 
8,  W.  line,  Kinnickinic,         -  10 
8,  mid.  W.  line,    -  30 

8,  mid.  W.  line,  S.  W.  qr.,    -  50 

9,  mid.  N.  line,  N.  W.  qr.,  35 
9,  N.  W.  qr.,  angle  in  road.  -  53 
9,  mid.  line,  road,  18 
9,  mid.  hue,  road  E.  and  W.,  38 
9,  S.  E.  qr.,  16 
9,  near  E.  line,  S.  E.  qr.,  R.  R.,  30 
9,  center  S.  E.  qr.,     -            -  51 

10,  N.  W.  qr.,  bank  of  lake,  25 

10.  S,  E.  qr.,  bank  of  lake,  -  25 

15,  N.  line,  bank  of  lake,  -  40 

15,  N.  line,  N.  W.  qr.,  Chic.  rd.  55 

15,  center,  -  75 
15,  Chicago  road,  N.  of  school 

house,  58 
15,  Chicago  road,  S.  of  school 

house,  75 

15,  S.  E.  qr.,  Deer  creek,  R.  R.,  60 

St.  Francis  R.  R.  station,  65 
Sec.  16,  mid.  W.  line,  N.  E.  qr.  of 

S.  E.  qr.,        -  57 

17,  N.  W.  corner,        -           -  57 

18,  mid.  N.  line,  N.  E.  qr.,  78 
18,  mid.  N.  line,                       -  82 
18,  N.  line,  N.  W.  qr.,  brook,  55 
18,  mid.  N.  line,  N.  W.  qr.,    -  86 
18,  N.  W.  corner,  -  83 
18,  mid.  W.  line,  N.  W.  qr.,  -  70 
18,  mid.  W.  line,    -  60 

18,  mid.  W.  line,  S.  W.  qr.,   -  90 

19,  N.  W.  corner,  -  102 
19,  mid.  W.  line,         -            -  113 
19,  W.  line,  S.  W.  qr.,  creek,  100 
19;  mid.  W.  line,  S.  W.  qr.,   -  125 


116 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN — continued. 


Lake.    T.  6,  R.  22  E.  —  (con.)  Feet. 

Sec.  20,  N.  W.  comer,    -  80 

20,  mid.  N.  line  N.  E.  qr.,  -    109 

20,  mid.  N.  line,  -  105 

20,  N.  line,  railroad,    -  -      86 

20,  mid.  W.  line  N.  W.  qr.,  79 

20,  mid.  S.  line  S.  W.  qr.,  -      97 

21,  mid.  N.  line  N.  E.  qr.,  72 
21,  mid.  N.  line,          -  -      78 
21,  mid.  N.  line  N.  W.  qr.,  83 

21,  N.  W.  corner,  100 

22,  N.  line,  Chicago  Road,  -      80 
22,  center  N.  E.  qr.,  Chicago  R'd,  82 

22,  mid.  line,  Chicago  Road,  -    100 
22, .S.  E.  qr.,  Chicago  Road,  90 

23,  N.  line,  bank  of  lake,-  -      30 
23,  N.  line,  Lake  Shore  Road,       45 
23,  mid.  N.  line,  -      35 
23,  W.line  S.W.qr.,  Chi.  Road,  120 
23,  N.  E.  qr.,  Lake  Shore  Road,  115 

23,  N.  line  S.  E.  qr.,  Lake  Sh.  R'd,  75 

24,  mid.  line,  bank  of  lake,  60 

25,  N.  line,  bank  of  lake,  -      80 
25,  N.  W.  corner,  90 
25,  mid.  W.  line,  -    102 

25,  mid.  line,  bank  of  lake,  80 

26,  mid.  N.  Line  N.  E.  qr.,  -      87 
26.  mid.  N.  line,  -  130 
26,  N.  line,  railroad,   -  -     113 
26,  N.  W.  corner,  116 

26,  mid.  W.  Line  N.  W.  qr.,  -      89 

27,  N.  line,  Chicago  Road,  124 
27,  mid.  W.  line,         -  -     122 
27,  N.  W.  corner,  83 
27,  mid.  line,  Chicago  Road,  84 

27,  center  S.  E.  qr.,  95 

28,  mid.  N.  line,          -  .  -      88 

28,  N.  W.  corner,  81 

29,  mid.  N.  line  N.  E.  qr.,  -      74 
29,  mid.  N.  line,    -  82 
29,  N.  Line,  railroad,    -  -      97 
29,  N.  W.  corner,  96 
29,  mid.  W.  line  N.  W.  qr.,  -    118 
29,  mid.  W.  line,  111 
29,  mid.  W.  line  S.  W.  qr.,  -    134 

29,  mid.  S.  line  S.  W.  qr.,  137 

30,  mid.  N.  line  N.  E.  qr.,  -     129 
30,  mid.  N.  line,  -            -  113 
30,  mid.  N.  line  N.  W.  qr.,  -     127 
30,  N.  W.  corner,  136 
30,  mid.  W.  line  N.  W.  qr.,  -     165 
30,  mid.  W.  line,  185 

30,  mid.  W.  line  S.  W.  qr.,  -     178 
81,  N.  W.  corner,  180 

31,  mid.  W.  line  N.  W.  qr.,  -     190 
81,  mid.  W.  line,  195 

31,  mid.  W.  line  S.  W.  qr.,  -    175 

32,  N.  line  N.  E.  qr.,       -  122 
32,  mid.  N.  line,          -  -    139 
32,  N.  line,  railroad,         -  137 
32,  N.  W.  corner,        -  -    142 

32,  mid.  S.  line  S.  W.  qr.,  154 

33,  mid.  N.  line  N.  E.  qr.,  -    103 
33,  mid.  N.  line,  -  115 
33,  mid.  N.  line  N.  W.  qr.,  -    102 


Lake.    T.  6,  R.  22  E.  — (con.)  Feet 

Sec.  33,  N.  W.  corner,  120 

34,  N.  line  N.  E.  qr.,  road,  -      98 

34,  mid.  N.  line,  -  90 

35,  N.  Hue,  railroad,    -  -HI 
35,  mid.  N.  line,  -  115 

35,  N.  E.  qr.,  angle  Chi.  Road,    108 

36,  N.  line  bank  of  lake,  -  90 
36,  mid.  N.  line  W.  hf,  N.  W. 

qr.,   -                        -  -     110 

36,  N.  W.  corner,  93 

Lake  Mills.    T.  7,  R.  13  E. 

Sec.   1,  W.  hf.,      -  -    265 

3,  center  N.  E.  qr.,  274 

3,  near  center  N.  W.  qr.,  -    327 

3,  mid,  W.  line  N.  W.  qr.,  311 

3,  S.  W.  corner,         -  -    291 

4,  center  N.  W.  qr.,        -  330 

4,  flat,  -    315 

5,  N.  E.  qr.,  hill,             -  370 

6,  S.  W.  qr.,  -    398 
8,  mid.  S.  line,    -  373 

Koshkonong  Creek  at  Kroughville,     257 

Sec.  10,  mid.  W.  line,  315 

Lake  Mills  village,  -    260 

Lake  Mills  village,  N.  W.  part,  277 

Rock  Lake,  -    250 

Sec.  18,  mid.  S.  line,    -  345 

19,  S.  W.  qr.,  creek,    -  -    288 
28,  mid.  S.  line  S.  E.  qr.,  278 
31,  S.  W.  qr.,  creek,    -  -     272 
33,  N.  E.  comer,  -            -  363 

La  Prairie.    T.  2,  R.  13  E. 

Sec.  13,  mid.  W.  line,  -  -  271 

16,  mid.  W.  line,  242 
Lima.  T.  4,  R.  14  E. 

Sec.   6,  S.  E.  qr.,  marsh,    -  -    243 

13,  N.  E.qr.,        -            -  307 

14,  S.  E.  qr.,    -            -  -    316 
18,  near  mid.  W.  line,      -  248 

21,  S.  E.  corner,  -    301 

22,  Lima  station,  -  310 

23,  mid.  N.  hf.,           -  -    305 
23,  W.  line,          -           -  308 
30,  E.  line,       -            -  -    311 

Lima.    T.  14,  R.  22  E. 
Sec.  2,  E.  line  S.  E.  qr.,  highland,     129 

16,  mid.  E.  line,  -     164 

20,  center  S.  E.  qr.,  219 
26,  center  N.  hf.,  -     119 

Hingham  Mill  Pond,  -  192 
Lincoln.  T.  25,  R.  24  E. 

Sec.  19,  S.  Line  outcrop,      -  -    232 

20,  S.  line  S.  W.  qr.,        -  192 

22,  mid.  S.  Line  S.  E.  qr.,  -     197 

23,  mid.  S.  line  S.  W.  qr.  (est.),  168 
26,  swamp,      -  -     114 
35,  stream,  98 

Linn.    T.  1,  R.  17  E. 

Sec.  5,  MoorfielcVs  lime  kiln,  -    368 

Geneva  lake,  -  282 
Little  Suamico.  T.  26,  R.  19  E. 

Sec.  26,  -  -  -  144 
Lowell.  T.  10,  R,  14  E. 

Sec.  6,  S.  W.  qr.,  -  -    256 


TOPOGRAPHY. 


117 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN — continued. 


Lowell.    T.  10,  R.  14  E.  —  (con.)  Feet. 

Sec.  7,  near  center  W.  hf.,    -  236 
15,  Lowell  Village, 

19,  N.  E.  qr.,        -  245 
30,  center  E.  hi,  R.  R., 
30,  near  S.  line  S.  E.  qr.,  marsh,  216 

Lowell  Station,        -  -    247 
Lowell.    T.  11,  R.  14  E. 
Sec.  26,  S.  E.  qr.,  ridge,      - 

30,  near  center  W.  hf.,     - 

31,  near  center  W.  hi'., 

36,  mid.  S.  line  S.  E.  qr.,  creek,  240 

36,  lull-top,      -  -    305 
Lynden.    T.  14,  R.  21  E. 

Sec.   1,  mid.  S.  line  S.  E.  qr.,  -    262 

2,  mid.  S.  line  S.  E.  qr.,  264 

3,  mid.  S.  line,  R.  R.,  -    224 

4,  mid.  S.  line,  valley,    -  245 
4,  S.  E.  comer,  Onion  River,  -    211 

6,  mid.  S.  line  S.  E.  qr.,  299 

26,  near  center, 

27,  mid.  S.  line,     -  352 

28,  mid.  E.  line  S.  E.  qr.,  stream,  278 
30,  near  mid.  W.  line,      -  433 
30,  S.  line  N.  E.  qr.,  stream,  -    305 
35,  N.  E.  corner,  church,  316 
35,  N.  line,  R.  R.,       -  -    307 

Cascade  River,  below  mill,      -  287 
Lyons.    T.  2,  R.  18  E. 

Lyons  Station,         -  -    222 
Sec.   1,  center  E.  line,  R.  R.,  - 

1,  near  mid.  S.  line,  -  -    291 

1,  S.  W.  qr.,        -            -  194 

1,  near  S.  W.  corner,  -    339 

2,  S.  W.  corner,  R.  R.,  -  200 

7,  S.  W.  qr.,  -  -    273 

8,  mid.  W.  line,  -  285 

9,  N.  E.  qr.,  -  -    228 
10,  N.  hf.,                        -  220 
10,  near  center  S.  line, 

12,  near  east  line,              -  355 

12.  S.  E.  qr.,  brook,     -  -    218 

23,  mid.  E.  line,    -           -  321 

23,  mid.  E.  line,  S.  E.  qr.,  -    355 

28,  S.  line  S.  E.  qr.,  319 

3Iagnolia.    T.  3,  R.  10  E. 

Magnolia  Station,   -  -    340 

Sec.  6,  mid.  W.  line  N.  W.  qr.,  354 

6,  mid.  W.  line,         -  -    285 

6,  S.  W.  qr.,  flat,            -  286 

6,  S.  W.  qr.,  -  -    309 

6,  S.  W.  qr.,  Allen's  Creek,  278 

6,  S.  E.  qr.,    -  -    360 
7S.E.qr-,         -  433 

7,  S.  E.  qr.,  road,       -  -    323 
7,  S.  E.  qr.,  top  of  ledge,  450 
9,  N.  W.  qr.,  Allen's  Creek,  -    292 

23,  N.  W.  qr.,      -  339 

26,  S.  W.  qr.,  -            -  -    384 

26,  S.  W.  qr.,  summit,     -  441 

28,  S.  W.  qr.,  -  -    339 

34,  N.  W.  qr.,      -  432 

Manitowoc.    T.  19,  R.  24  E. 

City,  S.  W.  corner,      -            -  60 

Station,       -  -        7 


Manitowoc.  T.  19,  R.  24  E.  —  (con.)  Feet. 

Sec.   5,  near  W.  line,  -  79 

6,  center  S.  W.  qr.,    -            -  69 

7,  N.  W.  qr.,  bridge, 

17,  N.  W.  cor.,  Little  Man'woc,  r> 

17,  S.  W.  qr.,  R.  R.,         -  44 

18,  N.  W.  qr.  S.  E.  qr.,  R.  R.,  :.l 

18,  S.  W.  qr  ,  R.  R.,        -  60 

19,  N.  W.  qr.,  R.  R.,  -            -  53 
Manitowoc  Rapids.    T.  19,  R.  23  E. 

Sec.   2,  mid.  S.  line  S.  W.  qr.,  1:16 

3,  near  S.  E.  corner,  -            -  153 

4,  mid.  E.  line,                      -  203 
4,  mid.  S.  line,  highland,  213 

4,  mid.  N.  line,  R.  R.,           -  154 

5,  mid.  E.  line,    -            -  158 

6,  mid.  E.  line,                      -  173 

10,  near  N.  line  S.  E.  qr.,  60 

11,  near  N.  line,                       -  124 

12,  near  mid.  W.  line,     -  75 

12,  mid.  S.  line  S.  W.  qr.,      -  68 

13,  center  N.  W.  qr.,  R.  R., 

13,  near  S.  E.  corner,  -            -  70 
19,  N.  E.  qr.,  top  of  Kettle's,  166 

19,  mid.  N.  W.  qr.,  river,        -  108 
22,  N.  line  N.  W.  qr.,      -  140 

24,  mid.  E.  line  N.  E.  qr.,       -  53 

25,  N.  W.  qr.  of  S.  E.  qr.,  R.  R.,  53 
32,  center  stream,        -            -  142 
34,  mid.  E.  hf.,  N.  shore  Sil.  L.  150 
34,  center  S.  E.  qr.,      -            -  129 

34,  S.  line  S.  E.  qr., 

35,  near  center,                        -  111 
Maple  Grove.    T.  20,  R.  21  E. 

Reedsville  Station,                          -  242 

Sec.  6,  328 

6,  S.  W.  corner,         -            -  329 

7,  Serpentine  ridge,        -  304 
12,  S.  E.  corner,           -            -  247 

29,  mid.  W.  line  S.  W.  qr.,  296 

30,  near  mid.  W.  line,              -  276 

32,  near  N.  E.  corner,      -  278 

33,  E.line,        -           -           -  276 

34,  E.  line,           -           -  262 

35,  S.  E.  corner,                        -  240 
Maple  Valley. 

Sec.  24,  N.  branch  LMe  River,  T.  29, 

R.  19  E.,      -  180 
Sec.  24,  Small  Lake,  T.  30,  R.  19  E.,  159 

25,  Little  Peshtigo  Lake,  -  157 
Marshfield.    T.  16,  R.  19  E. 

Sec.   6,  N.  W.  corner  (est.),     -  402 

6,  stream,       -                       -  360 

C,  S.  W.  corner,  -  406 

6,  S.  E.  corner,                       -  433 

14,  S.  E.  qr ,  Reichart  Quarry,  357 

16,  S.  line,  Maria  Hotel           -  365 

17,  N  line  (est.),  R.  R.,    -  371 
17,  S.  W.  corner,  hill,  -            -  442 

20,  near  center,  hill,    -           -  450 

24,  S.  E.  qr.,                      -  424 

25,  N.  line,      -                       -  420 
30,  S.  W.  qr.,  Staffer's  quarry,  409 

Calvary  station,      -                       -  363 

St.  Cloud  station,         -  349 


118 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OF  ELEVATIONS  AEOVE  LAKE  MICHIGAN  —  continued. 


Memee.    T.  17,  R.  22  E.  Feet. 

Sec.    1,  mid.  N.  line,  -     175 

5,  N.  W.  qr.,      -  -            848 
8,  N.  W.  corner,        -  -    348 

14,  S.  W.  qr.,  river,  135 

21,  mid.  N.  line,  -    248 

21,  center,  stream,  175 
Menasha.    T.  20,  R.  17  E. 

Menasha  station,  -     177 
Menomonee.    T.  8,  R.  20  E. 

Sec.   2,  N.  E.  qr.,  outcrop,  -    193 

6,  E.  side  N.  E.  qr.,  -  -    259 
8,  outcrop,  290 
8,  S.  line  S.  W.  qr.,  hill,  •    334 

Menomonee  Falls,  -    238-226 

Sec.  17,  center  N.  hf .,  -    314 

19,  N.  E.  qr.,  spring,  -            287 

30,  S.  W.  corner,  -    279 
Mention.    T.  9,  R.  21  E. 

Mequon  station,  92 

Thiensville  station,  -  88 

Sec.   1,  mid.  N.  line  N.  E.  qr.,  -     147 

10,  R.  R.,  -  128 

31,  N.  E.  corner,  valley,  -     154 

31,  N.  W.  corner,  252 

32,  N.  line,      -           -  -    172 
35,  R.  R.,  -           -  -           107 

35,  N.  W.  qr.,  R.  R.,  -  -      97 
T.  9,  R.  22  E. 

Sec.   5,  near  N.  E.  corner,  -     111 

5,  S.  line,  R.  R.,  93 

6,  mid.  N.  line,  river,  -      83 
8,  S.  line,  R.  R.,  98 

17,  S.  line,  R  R.,        -  -      94 

20,  mid.  N.  line,  bank  of  lake,     110 
20,  N.  W.  corner,        -  -      83 
29,  S.  line,       -  -    112 
32,  S.  line,  -              76 

Merton.    T.  8,  R.  18  E. 

Sec.  2,  yK  mi.  N.  of  Monches,  -    369 

Lake  Kessus,    -  376 

North  Lake,  -    309 

High  land  E.  of  Pine  Lake,  -            384 

High  land  W.  of  Pine  Lake,  -    345 

Ridge  1  mi.  W.  of  Pine  Lake,  359 
Valley  \Y2  mi.  W.  of  Pine  Lake,    -    318 

Metomen.    T.  15,  R.  14  E. 

Sec.  1,  N.  E.  qr.,  River's  quarry,  -    350 

Reed's  Corners  station,  407 

Brandon  station,     -  -    421 

Michicott.    T.  20,  R.  24  E. 

River  at  Michicott,  -      22 

Sec.   4,  S.  W.  qr.,       -  60 

8,  S.  hf.  of  S.  E.  qr,  T.  21,  126 

9,  E.  hf.  of  N.  E.  qr.,  rivei,          11 
22,  N.  W.  qr.,  -      53 

32,  S.  W.  qr.,  T.  21,  108 
Milford.    T.  8,  R.  14,  E. 

Hubbleton  station,  -  -    211 

Sec.  21,  mid.  N.  Ime,  -  260 

24,  N.  E.  corner,  -    232 

24,  mid.  S.  line,    -  222 

33,  N.  E.  qr.,  quarry,  -  -    284 

36,  center  N.  hf.,  -  295 
T.  7,  R.  14  E. 


Milford.    T.  7,  R.  14  E.  — (con.)  Feet. 

Sec.  6,  S.  E.  qr.,  outlet  of  lake,  -    228 

6,  S.  E.  qr.,  outcrop,        -  252 

Milton.    T.  4,  R.  13  E. 

Milton  station,        -  -    293 

Milton  Junction,  299 

Ridge  S.  of  Milton  Junction,  -     318 

Sec.  10,  S.  E.  comer,  -    216 

22,  center  E.  hf.,  hill,       -  375 

25,  S.  E.  qr.,    -            -  -     307 

26,  S.  E.  qr.,         -  303 
30,  N.  E.  qr.,        -  289 
30,  N.  W.  qr.,  -    255 

Milwaukee.    T  8,  R.  22  E. 

Sec.   4,  N.  line,  bank  of  lake,  -      87 

4,  mid.  W.  line,  93 

4,  center,        -  -      88 

5,  mid.  N.  line,  -  76 
5,  N.  W.  corner,        -  -      87 
5,  N.  W.  qr.,  Washington  R'd,  78 
5,  N.  line  S.  W.  qr.,  85 

5,  mid.  line  R.  R.,     -  -      84 

6,  mid.  N.  line,  -  107 
6,  mid.  N.  line,  N.  W.  qr.,  117 

6,  N.  W.  corner,        -  -     127 

7,  mid.  N.  line,  -  103 

7,  N.  W.  corner,        -  -      95 

8,  mid.  N.  line,  -  93 
8,  N.  W.  corner,        -  -      91 
8,  center  N.  E.  qr.,         -  79 

8,  center,        -  -      70 

9,  N.  line  R.  R.,  107 
16,  N.  line,  R.  R.,  127 
16,  mid.  line,  bank  of  lake,  -      93 

16,  mid.  line.,  R.  R.,        -  94 

17,  near  mid.  N.  line,  -       94 
17,  mid.  W.  line,  -  73 
17,  mid.  line,  Washington  Road,  91 

17,  N.  W.  corner,  -      62 

18,  N.  line,  river,  52 

19,  N.  line,  river,        -  49 
19,  mid.  N.  line,  -  65 
19,  N.  line,  Good  Hope,  -      90 
19,  N.  W.  corner,        -  -     120 
19,  W.  line,  N.  E.  qr.,  plank  rd.   70 

19,  mid.  line,  S.  E.  qr.,  plank-rd.  75 

20,  N.  W.  corner,        -  -      95 
20,  W.  line,  S.  W.  qr.,     -  42 
20,  W.  line,  river,  -      45 
20,  mid.  W.  line  N.  E.  qr.,  114 
20,  center  N.  E.  qr.,  120 

20,  mid.  line  Wash,  rd.,  -     105 

21,  N.  line,  M.  L.  S.  &  W.  R.  R.,  85 
29,  center  N.  E.  qr.,  -      70 
29,  W.  line,  river,  40 

29,  mid.  N.  ImeS.E.  qr.,  -       71 

30,  N.  W.  A.  R.  R.  &  G.  B.  rd.,     60 
30,  mid.  N.  line,  -      65 
30,  N.  line;  river  -  40 
30,  N.  W.  comer,         -  -    102 
30,  center,  50 

30,  center,  N.  E.  qr.,   -  -      55 

31,  mid.  N.  line,  50 
31,  N.  line,  creek,     -  -      40 
31,  mid.  N.  line  N.  W.qr.,  50 


TOPOGRAPHY. 


119 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Milwaukee.    T.  8,  R.  22  E.  —  (con.)  Feet. 

Sec.  81,  N.W.  corner,         -  -      60 

31,  R.  R.  bridge,  Milwaukee  R.,    51 
Lindwurm  station, 
Sec.  32,  mid.  N.  line, 

33,  N.  line  bank  of  lake,  -  80 

33,  IST.  line  R.  R.,  -      73 

33,  N.  W.  corner,  73 

33,  mid.  W.  line,  -      74 
33,  mid.  N.  E.  qr.,  bank  of  lake,  75 

33,  N.  line,  bank  of  lake,  -      80 

33,  mid.  line,  S.  E.  qr.,     -  75 
Milwaukee.    T.  7,  R.  22  E. 
Sec.   3,  N.  line,       - 

3,  N.  W.  corner,  92 

3,  mid.  W.  line, 

3,  center  N.  E.  qr.,  bank, 

3,  mid.  line,  bank,     -  -     108 

3,  center  S.  E.  qr.,  bank,  110 

4,  mid.  N.  line  N.  E.  qr.,  -      93 
4,  N.  line  R.  R.,  71 
4,  mid.  N.  line,  -      64 
4,  W.  line,  river 

4,  center  S.  W.  qr.,  river, 

4,  N.  W.  corner,        -  -      59 

5,  N.  line  R.  R.,  57 
5,  N.  line  N.  E.  qr.,  -      59 
5,  mid.  N.  line, 

5,  N.  W.  corner,  river,  -      37 

5,  W.  line  R.  R.,  98 

5,  W.  line,  Green  Bay  rd.,  114 

5,  center,        -  -      71 

5,  mid.  line  R.  R.            -  80 

5,  mid.  line,  river,      -  -      36 

6,  N:  line,  Green  Bay  road,  68 
6,  mid.  N.  line,  -      70 
6,  N.  W.  corner,              -  66 
6,  center  N.  E.  qr.,     - 

6,  R.  R.  &  Green  Bay  road,  98 

7,  mid.  W.  line, 

7,  mid.  line  near  S.  line,  124 

8,  mid.  N.  line,  -      94 
8,  N.  line,  Green  Bay  road, 

8,  W.  of  center,  155 

9,  Humbolt  Junction  -      61 
9,  mid.  N.  line,  -            -  84 

River  at  Humbolt  Bridge,  -      15 
Sec.    9,  mid.  W.  line  N.  E.  qr., 

9,  center,  -      63 

9,  mid.  W.  line  R.  R.,    -  90 

10,  N.  line,  bank  of  lake,  -    102 

10,  N.  W.  corner,  90 

10,  mid.  W.  line,  -      47 

10,  mid.  W.  line,  S.  W.  qr.,  78 
10,  center  N.  E.  qr.,  Lake  Ave.,  105 

10,  mid.  line,  Lake  Avenue,  -      83 

10,  S.  E.  qr.,  Lake  Avenue,  98 

10,  S.  line,  Lake  Avenue,  -      88 

Mitchell.    T.  14,  R.  20  E. 

Sec.    2,  near  mid.  S.  line,        -  580 

9,  S.  E.  corner,  high  hill,  -  566 

10,  S.  E.  corner,  -    510 

21,  mid.  E.  line,  491 

27,  N.  W.  qr.,  Stanley  Creek,  391 


Montpelier.    T.  23,  R.  23  E. 
Sec.  25,  near  center, 

25,  mid.  S.  line  S.  E.  qr.,  - 
Morrison.    T.  21,  R.  21   E. 

Sec.  28,  N.  W.  comer,  Diy  Run, 
34,  mid.  W.  line,  stream, 
34,  mid.  S;tone, 
MoseJ.    T.  16,  R.  23  E. 
Sec.   4,  S.  line  R.  R., 

5,  mid.  S.  line,  stream, 
5,  S.  line  S.  W.  qr., 


Feet. 

I?.S 


240 

284 

51 

112 


A* 

r 


16,  mid.  N.  line  N.  E.  qr.  R.  R.,    51 

16,  N.  line  N.  W.  qr.,  stream,        56 

27,  mid.  1ST.  line,  -      50 
Bank  three-qr.  mile  N.  of  pier,             48 

Mount  Pleasant.    T.  3,  R.  22  E. 

Sec.   4,  N.  W.  corner,  -            -    150 

4,  near  mid.  S.  line,  -            147 

9,  near  mid.  S.  line,  -    158 

12,  N.  E.  qr.,        -  105 

17,  center,        -  -    151 
20,  S.  E.  qr.,         -  158 
20,  S.  hf.,  -     178 

W.  U.  Junction,  143 

Sec-  21,  S.  E.  qr.,  -    126 

22,  S.  E.  qr.,  95 

23,  E.hf.,         -  -           -    120 

25,  N.  W.  corner,  141 

26,  N.  W.  corner,  -            -      92 

28.  mid.  S.  line,    -  129 
30,  N.  E.  qr.,  -  -     168 
30,  N.  W.  qr.,  Windsor,  203 

—  T.  3,  R.  22  E. 

Sec.   5,  S.  line,        -  -      45 

19,  S.  E.  corner,  80 

19,  N.  E.  qr.,     -  -      78 

20,  S.  line, 

21,  Racine  Junction,  - 
Vaughn's  Quarry,         -  58 
Horkck's  quarry,     -  -                   46 
Sec.  32,  center,  38 

32,  S.  line,        -  -      40 
Mukwonago.    T.  5,  R.  13  E. 

Sec.    6,  marsh,        -  -    305 

14,  S.  W.  comer, 

Mukwonago  village,  -    276 
Muskego.    T.  5.  R.  20  E. 

Sec.  13,  mid.  E.  line,  -  205 

13,  mid.  S.  line,  -    227 

33,  near  mid.  S.  line,  -            191 
Muskego  lake,        -  -    191 

Newark.    T.  1,  R.  11  E. 

Sec.    1,  N.  E.  qr.,  spring,  -            258 

1,  S.  W.  qr.,            -  -    362 

3,  N.  W.  qr.,      -  328 

10,  mid.  W.  line,  -           -    342 

11,  S.  W.  qr.,      -  357 
11,  S.  W.  qr.,  hill,  - 

13,  W.  line  near  mid.,  -            313 

13,  S.  E.  corner,  -    263 

13,  S.  E.  qr.,  flat,  193 

14,  N.  W.  qr.,  -    305 

14,  S.  W.  qr.,       -  -            331 

15,  S.  W.  qr.,  stream,  -    296 

16,  S.  E.  .corner  of  S.  W.  qr.,       244 


120 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Newark.    T,  1,  R.  11  E.  —  (con.)  Feet. 

Sec.  16,  S.  W.  qr.,  Coon  creek,  -     183 

20,  mid.  S.  line,  ridge,      -  318 

24,  N.  E.  qr.,  stream,  -  -     196 

25,  center  W.  hi,  252 

25,  S.  E.  qr.,    -  «ft      -  -    274 

28,  N.  E.  qr.,  cri*,  190 

29,  N.E.  qr.,  quarry,   -  -    222 
31,  center  E.  hf,    - 

31,  near  center,  -    263 

31,  W.  of  center,  275 

31,  W.  hf,       -  -    249 

32,  center,  281 

33,  near  center,  -    207 
33,  mid.  W.  line,      .         -  220 

33,  bottom  of  outcrop,  -    245 

34,  center,  ridge,  -  207 

35,  center,  creek,  -     144 
New  Berlin.    T.  6,  R.  20  E. 

Sec.  21,  mid.  N.  hf,     -  291 

22,  general  level  E.,    -  -    3SQ 
32,  N.  W.  corner,  Prospect  hill,    344 

New  Denmark.    T.  22,  R.  22  E. 

Sec.    7,  N.  E.  qr.,  Two  Rivers,  -    218 

17,  N.  line  N.  W.  qr.,     -  295 

28,  near  N.  W.  corner,  -    328 

35,  S.  W.  qr.,  Kettle  range,  307 
New  Holstein.    T.  17,  R.  20  E. 

Sec.  30,  S.  W.  qr.,       -  484 

32,  N.  W.  corner,        -  -    402 

34,  N.  W.  qr.,      -           -  426 
Newton.    T.  18,  R.  23  E. 

Sec.  1,  N.  line,  R.  R.,      -  -      77 

1,  creek,  52 

4,  S.  line  S.  E.  qr.  of  S.  W.  qr.  190 

12,  N.  line  R.  R.,  -    79 

13,  N.  line  R.  R.,             -  85 

17,  -    166 

23,  N.  line  R.  R.,  80 

26,  N.  line  R.  R.,        -  -      74 

27,  creek,  57 

30,  mid.  W.  line,  S.  W.  qr.,  140 
34,  N.  line  R.  R.,        -  -      77 

Norway.    T.  4,  R.  20  E. 

Wind  lake,  -    190 

Sec.    8,  N.  line,  198 

8,  S.  line,        -  -     198 

18,  S.  E.  corner,     -  221 

19,  S.  W.  corner,        -  -    224 
Oak  Creek.    T.  5,  R.  22  E. 

Sec.    1,  N.  line,  bank  of  lake,  -      80 

1,  N.  W.  corner,  75 

2,  mid.  N.  line,  -      90 
2,  N.  line  R.  R.,  96 

2,  mid.  line  N.  W.  qr.,  -     112 

3,  mid.  N.  line,  122 

3,  N.  W.  corner,        -  -      96 

4,  mid.  N.  line,  115 
4,  mid.  N.  line  N.  W.  qr.,  -    149 

4,  N.  W.  corner,        -  161 

5,  mid.  N.  line,  149 
5,   mid.  N.  line,  N.  W.  qr., 

Lake  station,      -  -    154 
5,  mid.  N.  line  W.  hf .  N.  W. 

qr.,  -     160 


Oak  Creek.  T.  5,  R.  22  E.— (con.)  Feet. 

Sec.  5,  N.  W.  corner,  152 

5,  mid.  W.  line  N.  W.  qr.,  -     104 

5,  mid.  W.  line,  161 

5,  mid.  W.  line  S.  W.  qr.,  -     158 

6,  N.  W.  corner,  185 
6,  mid.  W.  line  N.  W.  qr.,  -    205 

6,  mid.  W.  line,  210 

7,  mid.  N.  line  N.  E.  qr.,  -     160 
7,  mid.  N.  line,  175 
7,  mid.  N.  line  N.  W.  qr.,  -     170 
7,  N.  W.  corner,  195 
7,  mid.  W.  line  N.  W.  qr.,  -     180 

7,  mid.  W.  line,  175 

8,  mid.  N.  line  N.  E.  qr.,  -     133 
8,  mid.  N.  line,  150 
8,  N.  line  R.  R.,        -  -    147 
8,  N.  W.  corner,              -  155 

8,  near  mid.  S.  line,    -  -     129 

9,  mid.  N.  line  N.  E.  qr.,  96 
9,  mid.  N.  line,  -     111 
9,  mid.N.  line  N.  W.  qr.,  155 
9,  N.  W.  corner,        -  -    134 

10,  N.  line,  Oak  creek,     -  71 

10,  mid.  N.  line  N.  E.  qr.,  -      80 

10,  mid.  N.  line,  119 

10,  mid.  N.  line,  N.  W.  qr.,  -    138 

10,  N.  W.  corner, 

11,  N.  line,  Oak  creek,  -  -    45 
11,  N.  line,  Chicago  road,  -      74 
11.  N.  line,  R.  R,,  94 
11,  N.  line  N.  W.  qr.,  -     111 
11,  N.  W.  corner,  82 
11,  center,  Oak  Creek  station,        86 

11,  mid.  line,        -  107 

12,  N.  line,  bank  of  lake,  -      80 
12,  mid.  W.  line  N.  E.  qr., 

12.  N.  W.  corner,        -  -      65 

14,  N.  line,  Chicago  road,  108 

14,  mid.  N.  line  N.  W.  qr.,  -      89 

14,  N.  W.  corner,  105 

15,  mid.  N.  line  N.  E.  qr.,  -      91 
15,  mid.  N.  line,  -  96 
15,  N.  W.  corner,        -  -     102 
15,  mid.  N.  line  N.  W.  qr.,  126 
15,  mid.  W.  line  S.  E.  qr.,  -      88 
15,  mid.  W.  line  N.  E.  qr.,  101 

15,  center,        -  -     112 

16,  N.  line,  Oak  Creek,    -  77 
16,  mid.  N.  line  N.  E.  qr.,  -      77 
16,  mid.  N.  line,  -  91 
16,  mid.  N.  line  N.  W.  qr.,  -     113 
16,  N.  W.  corner,  142 
16,  mid.  W.  line  N.  W.  qr.,  -     134 
16,  mid.  W.  line,  136 

16,  mid.  W.  line  S.  W.  qr.,  -    122 

17,  mid.  N.  line  N.  E.  qr.,  130 
17,  mid.  N.  line,  R.  R.,  -     129 
17,  mid.  N.  line  N.  W.  qr.,  136 
17,  N.  W.  corner,        -  -     140 
17,  mid.  W.  line  N.  W.  qr.,  125 
17,  mid.  W.  line,  -     130 
17,  mid.  W.  line  S.  W.  qr.,  140 
17,  mid.  W.  line  S.  hf.  S.W.  qr.,  155 
17.  mid.  S.  line  S.  W.  qr.,  -     116 


TOPOGRAPHY. 


121 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Oak  Creek.    T.  5,  R.  22  E.  —  (con.) 
Sec.  18,  N.  W.  comer, 

20,  mid.  N.  line  N.  E.  qr.,      - 

20,  mid.  N.  line,  - 

20,  N.  line,  R.  R., 

20,  mid.  N.  line  N.  W.  qr., 

20,  N.  W.  corner, 

20,  mid.  S.  line  S.  W.  qr., 

21,  N.  W.  corner, 

22,  mid.  N.  line  N.  E.  qr., 

22,  mid.  N.  line, 

23,  N.  line,  R.  R., 
23,  mid.  N.  line, 

23,  mid.  N.  line  N.  W.  qr., 

23,  N.  W.  corner, 

23,  mid.  line,  R.  R., 

23,  mid.  line,  Chicago  road,     - 

23,  cent.  N.  hf .  S.E.  qr.,  Ch.  rd 

26,  N.  line,  Chicago  road, 

26,  mid.  line,  Chicago  road, 

27,  mid.  W.  line, 

27,  mid.  W.  line  S.  W.  qr., 

28,  mid.  N.  line, 

28,  mid.  N.  line  N.  W.  qr., 
28,  N.  W.  corner, 
28,  mid.  N.  line  S.  E.  qr., 
28,  center,        - 

28,  mid.  W.  line  N.  E.  qr., 

29,  mid.  N.  line  N.  E.  qr., 
29,  mid.  N.  line,  - 

29,  mid.  N.  line  N.W.  qr.,  R.  R 
29,  N.  W.  corner, 

29,  mid.  S.  line  S.  W.  qr., 

30,  mid.  N.  line  N.  E.  qr.,      - 
30,  mid.  N.  line,  - 

30,  mid.  N.  line  N.  W.  qr.,    - 
30,  N.  W.  corner, 
30,  mid.  W.  line  N.  W.  qr.,    - 
30,  mid.  W.  line, 

30,  mid.  W.  line  S.  W.  qr.,     - 

31,  mid.  N.  line  N.  E.  qr., 
31,  mid.  N.  line, 

31,  mid.  N.  line  N.  W.  qr., 

31,  N.  W.  comer, 

32,  mid.  N.  line  N.  E.  qr., 
32,  mid.  N.  line, 

32,  mid.  N.  line  N.  W.  qr., 

32,  N.  W.  corner, 

33,  rtid.  N.  line  N.  E.  qr., 
33,  mid.  N.  line, 

33,  mid.  N.  line  N.  W.  qr., 

33,  N.  W.  comer, 

34,  mid.  N.  line  N.  E.  qr., 
34,  mid.  N.  line, 

34,  mid.  N.  line  N.  W.  qr., 

34,  N.  W.  corner, 

34,  mid.  W.  line  N.  W.  qr., 

34,  mid.  W.  line, 

34,  mid.  N.  line  S.  W.  qr., 

34,  center, 

34,  mid.  N.  line  S.  E.  qr., 

35,  mid.  N.  line  N.  E.  qr.,      - 
35,  mid.  N.  line,  - 

35,  mid.  N.  line  N.  W.  qr.,    - 
35,  N.  W.  corner, 


Feet. 
160 
125 
143 
116 
130 
140 
111 
121 
104 
83 
105 
111 
103 
119 
110 
116 
,,  127 
117 
128 
85 
94 
87 
108 
99 
94 
106 
112 
108 
100 
,,111 
111 
105 
110 
113 
124 
120 
110 
132 
136 
133 
136 
147 
150 
145 
135 
105 
119 
100 
110 
125 
133 
87 
88 


94 
92 
85 
88 
81 
79 
105 
95 
91 
86 


Oak  Creek.    T.  5,  B.  22  E.  —  (con.)  Feet, 

Sec.  35,  mid.  W.  line,  -       77 
35,  mid.  N.  line  S.  W.  qr., 

35,  center,        -  -      78 

35,  mid.  N.  line  S.  E.  qr.,  96 

36,  N.  W.  corner,        -  -    114 
36,  mid.  W.  line,  -  104 
36,  mid.  W.  line  S.  W.  qr.,  -     102 
36,  mid.  S.  line  S.  W.  qr.,  118 
36,  laid.  S.  line, 

36,  S.  line,  R.  R.  station,  117 
36,  Chicago  rd.  on  County  line,    110 

36,  S.  E.  corner,  -    130 
Top  of  bank  (Sec.  31,  T.  5,  R.  23),       80 
Oak  Grove.    T.  11,  R.  15  E. 

Horicon  Junction,    -  -    306 
Minnesota  Junction,     - 

Rolling  Prairie  station,       -  -    363 

Juneau  station,  335 
Oakland.    T.  6,  R.  13  E. 

LakeRipley,    -           -           -  239 
Red  Cedar  lake,     - 

Sec.  4,  S.  W.  qr.,  -  -    266 

5,  S.  half,  280 

7,  W.  line  N.  W.  qr.,  -    271 

13,  mid.  W.  line  N.  W.  qr.,  -    343 

16,  S.  E.  corner,    -  330 

18,  S.  E.  qr.  of  S.  E.  qr.,  -    246 

19,  near  TS.  W.  corner,     -  264 
19,  center  S.  E.  qr.,     -  -    251 

19,  S.  W.  qr.,       -           -  234 
25,  near  N.  W.  corner, 

25,  W.  line  N.  W.  qr.,     -  270 
28,  mid.  E.  line, 

28,  near  mid.  S.  line,        -  227 

30,  S.  W.  qr.,  -    257 

30,  near  center  S.  W.  qr.,  253 

31,  S.  W.  qr.,  -    214 

31,  S.  lineS.  W.  qr.,        -  210 
Oconomowoc.    T.  8,  R.  17  E. 

Lac  La  Belle,  -    273 

Oconomowoc  station,    -            -  283 

Osceola.    T.  14,  R.  20  E. 

Sec.   1,  mid.  W.  line,         -  -    500 

4,  N.  E.  qr.,  cross  roads,  458 

11,  S.  W.  qr.,  stream,  -    453 

13,  Long  Lake,     -  443 

30,  E.  hf.,  pond,  -    413 

32,  N.  line,  518 

34,  general  level,  -    50-i 

35,  N.  hf.,  Canton,  566 
Palmyra.    T.  5,  R.  16  E. 

Palmyra  station,     -  260 

Sec.  20,  E.hf.,  266 

20,  N.  W.  qr.,  -    278 

22,  S.  E.  qr.,         - '  290 

23,  N.  E.  qr.,  -  -    271 

28,  N.  line,  241 

29,  S.  E.  qr.     -            -  -    220 

31,  center,            -  221 

32,  W.  line,      -  -    221 
Paris.    T.  7,  R.  21  E. 

Sec.  18,  center,  praine,             -  191 
Pensaukee.    T.  27,  R.  19  E. 
Sec.  23,  N.  branch,  Pensaukee  road,   139 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OP  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Pensaukee.  T.  27,  R.  19  E.  —  (con.)  Fee.l. 

Sec.  35,  Pensaukee  river,  128 

Pewaukee.    T.  7,  R.  19  E. 
Pewaukee  Lake,      ...    263 

Pewaukee  station,        -  263 

I.  N.  Stewart's  place,         -  -    316 

Sec.    1,  center,  262 

12,  highland,    -  -    358 

12,  mid.  S.  line,    -            -  268 

13,  niid.  N.  hf.,           -  -    254 
16,  S.  E.  qr.,  284 
26,  quarry,       -  -    248 
26,  railroad  crossing,        -  248 
32,  W.  hf.,       -           -  -    330 

Pierce.    T.  24,  R.  24  E. 

Gen.  level,  E.  of  Casco  village,  203 

Sec.  28,  center,  high  bluff,  -  -    188 

28,  river,    -  30 
32,  N.  E.  qr.,  -  -      44 
32,  N.  E.  qr.,  top  of  Wilmot's 

quarry,  126 

32,  N.  E.  qr.,  outcrop,  -      61 

32,  N.  E.  qr.,  above  outcrop,  77 

33,  S.  W.  qr.,        -  179 
Pierce.    T.  24,  R.  25  E. 

4J^  miles  S.  W.  of  Ahnapee,  -  144 

Bank  at  Alaska,      -  58 

Sec.  20,  N.  W.  qr.,      -  141 

31,  S.  E.  corner,  -      99 
Pleasant  Prairie.    T.  1,  R.  22  E. 

Kenosha  Junction,       -  101 

Pleasant  Prairie  station,     -  -     119 

Eau  Pleine  river,  near  state  line,  77 

Sec.   1,  mid.  N.  line  N.  E.  qr.,  -      50 

1,  mid.  W.  line,  70 

1,  S.  W.  qr.,  -      44 

2,  mid.  S.  line  S.  W.  qr., 

4,  near  mid.  N.  line,  -     100 

4,  near  mid.  S.  line,        -  101 

7,  W.  line,      -            -  -    106 

9,  mid.  N.  line,  railroad,  101 

10,  W.  line,     -            -  -     120 

16,  W.  line,          -  150 

16,  mid.  S.  line  S.  W.  qr.,  -      98 

18,  Eau  Pleine  river,        -  73 

20,  mid.  S.  line  S.  E.  qr.,  -      97 

24,  N.  E.  qr.,        -  72 

29,  mid.  S.  line  S.  E.  qr.,  -      95 

32,  mid.  S.  line  S.  E.  qr.,  90 

32,  center  E.  hf.,  railroad,  -      93 

33,  S.  E.  corner,    -  134 
35,  40  rods  W.  of  mid.,  S.  line,    160 

Pleasant  Prairie.    T.  1,  R.  23  E. 

Sec.  18,  S.  E.  qr.,  beach  I,  -      26 

18,  S.  E.  qr.,  beach  II,     -  39 

31,  S.  W.  qr.,  beach  III,  -      64 

Beach  I,  near  state  line,  34 

Beach  II,  near  state  line,    -  55 
Plymouth.    T.  2,  R.  11  E. 

Hanover  Junction,       -  209 

Sec.   1,  S.  W.  qr.,  -    261 

9,  N.  E.  corner,  railroad,  225 

28,  mid.  W.  line,         -  -    395 

33,  N.  E.  corner,  342 

35,  mid.  W.  line,         -  -    412 


Plymouth.    T.  15,  R.  21  E.  Feet. 

Plymouth  station,         -  262 

Red  Clay,  E.  of  Plymouth,  -    305 

Sec.  3,  N.  W.  qr.,'      -  343 

16,  S.  E.  qr.,  stream,  - 

31,  S.  line.  Onion  river,    -  232 

32,  S.  E.  qr.,  1st  Kettle  Ridge,    309 

33,  S.  line  S.  E.  qr.,     -  -    340 

34,  S.  line,  railroad  crossing,  224 
36,  S.  E.  corner,  hill,   -  -     253 

Polk.    T.  10,  R.  19  E. 

Cedar  Creek  village,    -  481 

Cedar  Lake,  -    442 

Schleisingerville  station,  474 

Ackerville  station,  -  -    480 

Sec.   6,  mid.  N.  line  N.  W.  qr.,  448 

6,  N.  line  N.  E.  qr.,  -    480 

6,  N.  E.  corner.  -  r.(.)4 

33,  mid.  E.  line,  -    535 
Porter.    T.  4,  R.  11  E. 

Sec.   1,  N.  E.  corner,  -    284 

3,  N.  E.  qr.,  Catfish  river,  196 

3,  N.  line  N.  W.  qr.,  -    265 

3,  S.  W.  qr.,  stream,       -  196 

5,  N.  E.  corner,  -    247 

5,  mid.  N.  line  N.  W.  qr.,  261 

6,  mid.  E.  line,  -    261 
9,  N.  W.  qr.,      -  250 
9,  mid.  E.  line  N.  E.  qr.,  -    2uO 

Portland.    T.  9,  R.  13  E. 

Crawfish.  E.  of  Portland,        -  214 

Sec.    1,  N.  W.  corner,        -  -     250 

6,  N.  W.  qr.,      -  296 

6,  N.  W.  qr.,  marsh,  -    286 

6,  center  W.  hf.,  307 

7,  W.  line  N.  W.  qr.,  marsh,     276 

8,  mid.  W.  hf.,  stream,  -     259 

17,  near  mid.  S.  line,  marsh,  241 

18,  mid.  N.  line,  -    268 

18,  N.  W.  corner,  297 

19,  N.  W.  qr.,  marsh,  -    244 
27,  N.  hf.,                        -  253 
27,  N.  W.  qr.,  Crawfish,  -    221 
27,  top  of  conglomerate,  269 
29,  center  E.  hf.,  -    259 
29,  near  S.  line,    -  279 
31,  N.  E.  corner,  -    290 
31,  near  mid.  N.  line,       -  270 
31,  N.  W.  corner,        -  -    340 
31,  S.  E.  corner,  308 

34,  mid.  N.  line  N.  W.  qr.,  -    330 

35,  S.  W.  qr.,       -  219 

35,  mid.  E.  line,  -    214 

36,  mid.  N.  line  S.  W.  qr.,  295 
Preble.    T.  24,  R.  21  E. 

Top  of  beach  line,  1  mi.  E.  of  Green 

Bay,         -  -      14 

Sec.  26,  mid.  E.  line,  -  152 

27,  fork  of  roads,         -  -      25 

33,  mid.  of  W.  line,  11 

34,  N.  W.  qr.,  -      59 
34,  top  of  highland,  155 

34,  center,  highland,    -  -     144 

35,  S.  E.  qr.,  gen.  level  of  high- 
land,     -  157 


TOPOGRAPHY. 


123 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN — continued. 


Preble.    T.  24,  R.  21  E.  —  (con.)  Feet. 

Sec.  36,  N.  E.  qr.,  -  -    189 

36,  mid.  N.  hf.,     -  180 

9,  S.  hi,  T.  23,  -      91 

Randall.    T.  1,  R.  19  E. 

Lake  Elizabeth,      -  -     196 

Sec.  18,  Power's  Lake,  265 

18,  S.  E.  corner,  -     282 

19,  mid.  S.  line,    -  289 
21,  E.  hf.,  R.  R.,         -  -    201 

35,  mid.  S.  hf.,     -           -  298 

36,  S.  hf.  of  S.  E.  qr.,  -    340 
Rantoul.    T.  19,  R.  20  E. 

Sec.  4,  mid.  E.  line  (est.),        -  271 

Hilbert  Station,      -  -    250 

School  house  S.  of  Hilbert,      -  301 
Raymond.    T.  4,  R.  21  E. 

Sec.    7,  mid.  W.  line,        -  -    203 

18,  S.  W.  corner,  2:38 

21,  N.  W.  qr.,              -  -     179 

36,  N.  line  N.  E.  qr.,        -  89 
Red  River.    T.  25,  R.  23  E. 

Mayville  beds  in  N.  part  of  town,  163 

Sec.  20,  S.  E.  qr.,   -  -     186 
21,  S.  line  S.  E.  qr., 

21,  S.  E.  qr.,  smooth  thin  beds,   138 

22,  S.  E.  qr.,    -  -     168 

22,  mid.  S.  line,  highland,  249 

23,  S.  line  S.  W.  qr.,  swamp,  176 

24,  S.  line  S.  W.  qr.  (?),  outcrop,  268 
27,  N.  W.  qr.,  -    203 

33,  N.  line  JST.  E.  qr.,  stream,  125 

34,  N.  W.  qr.  N.  line,  stream,  144 

35,  N.  W.  corner,  highland,  -    274 

36,  N.  E.  comer,  gen.  level,  285 
Rhine.    T.  16,  R.  21  E. 

Elkhart  Station,     -  -    362 

Sec.    1,  mid.  N.  E.  qr.,  341 

13,  N.  E.  corner,  -    211 

18,  center  E.  hf.,  R.  R.,  316 

19,  S.  E.  qr.,  summit,  -    426 
24,  E.  line  N.  E.  qr.,        -  327 
33,  S.  W.  qr.,  stream,  -    300 

Richfield.    T.  9,  R.  19  E. 

Richfield  Station,    -  -    381 

Sec.   3,  mid.  E.  line,  413 

3,  20  rods  W.  of  mid.  E.  line,    542 

4,  mid.  E.  line,  -    528 
10,  mid.  E.  line,   -  530 
15,  S.  E.  corner,  -    430 
22,  S.  line,  Bark  river,      -  367 
22,  S.  E.  qr.,    -  -    498 
26,  N.  E.  qr.,        -  379 
36,  N.  E.  corner,  -    429 
86,  E.  line  of  S.  E.  qr.,    -  300 

Rippn.    T.  16,  R.  14  E. 

Ripon  Station,        -  -    352 

Cliff,  W.  of  road,        -  341 

City.    Falls  under  tressel  bridge,  332 

Top  of  St.  P.,  near  limekiln,  351 

Top  of  Hill,  W.  of  limekiln,  373 

St.  Peters,  W.  of  last,  -    358 

Coombs  quarry,  bottom,  370 

Sec.   2,  (est.),  S.  E.  corner,  -    309 

19,  mid.  W.  line,          -  304 


Ripon.    T.  16,  R,  14  E.  —  (con.)        Feet. 

Sec.  20,  N.  W.  qr.  of  N.  W.  qr.,  -  327 

20,  N.  W.  of  center,  quarry,  40l) 

20,  little  W.  of  center,            -  397 

20,  near  mid.  S.  line,         -  350 

20,  S.  W.  qr.  of  S.  E.  qr.,       -  351 

20,  N.  E.  qr.  of  S.  W.  qr.,  381 

21,  Quarry  S.  W.  of  Mr.  Starr's,  364 
26,  N.  W.  qr.,                  -  366 

28,  N.  line  N.  E.  qr.,  -            -  370 

29,  N.  E.  qr.  near  center,  350 
29,  N.  E.  qr.,  top  of  limestone,  370 
29,  20  rods  S.  of  last,  -            -  341 

35,  S.  E.  qr.,         -  364 

36,  S.  E.  qr.,  stream,  -            -  343 
Rochester.    T.  3,  R.  19  E. 

Sec.   2,  mid.  S.  line,    -           -  203 

14,  N.  E.  qr.,  river,     -            -  187 

15,  S.  E.  qr.,  bluff,  276 
15,  mid.  S.  line  S.  E.  qr.,  200 

Rock.    T.  2,  R.  12  E. 

Afton                                              -  206 

Sec.   7,  N.  E.  qr.,  summit,  306 

8,  N.  W.  qr.,  R.  R.,  marsh,  265 
20  mid.  W.  line,  Bass  creek  flat  183 

2i;  mid.  W.  line,         -           -  206 
Rockland.    T.  19,  R.  21  E. 

Rockland  ledge,      -            -            -  300 

Sec.  4,  S.  E.  qr.,  outcrop,       -  310 

4,  mid.  E.  line,       -                -  258 

Rockland.    T.  22,  R.  20,  E. 

Sec.   3,  N.  hf.,       -                      -  22 

3,  S.  E.  qr.  E.  of  east  river,  30 
14,  mid.  E.  line,  base  of  ledge,  267 
24,  mid.  E.hf.,  level  above  ledge  320 

Rosendale.    T.  16,  R.  15  E. 

Rosendale  station,                          -  313 

West  Rosendale  station,          -  :104 

Rubicon  station,                               -  440 

Sec.   4,  S.  W.  qr.,       -  288 

4,  S.  W.  qr.,  quarry,              -  278 
28,  N.  W.  qr.,  river,         -  271 
32,  S.  E.  corner,  345 

Russell.    T.  16,  R.  20  E. 
Sec.  31,  W.  lineN.  W.  qr.,  Sheb.riv.  325 

36,  E.  line  S.  E.  qr.,  hill,         -  244 

Salem.    T.  1,  R.  20  E. 

Salem  station,  198 

Fox  river  station,    -                        -  200 

Fox  river  at  Wilmot,                -  154 

Sec.  32,  N.  E.  qr.,  -           -           -  161 

Saukville.    T.  11,  R.  21  E. 

Saukville  station,  181 

Sec.   2,  E.  line  S.  E.  qr.,    -           -  249 

26,  N.  E.  qr.,  quarry,        -  212 

34,  mid.  S.  line,  outcrop, 

35,  S.  line,  R.  R.  crossing,  181 
Schleswig.    T.  17,  R.  21  E. 

Rockville,                            -           -  286 
Sheboygan  river  under  bridge  be- 
tween Rockville  and  Kiel,           -  272 
Kiel  station,  333 
Sec.   6,  N.  E.  qr.,  gen.  level,         -  295 
17,  N.  W.  corner,  gen.  level,  330 
20,  N.  W.  qr.,      -  359 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OP  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Scott.    T.  13,  R.  20  E.  Feet 

Sec.   9,  Stanley  creek,     -         -  32 

10,  -    326 

19,  Tamarac  swamp,        -  39! 

27,  mid.  N.  line,  -    328 

27,  Stanley  creek,  284 
Scott.     T.  24,  R.  22  E. 

Sec.   7,  W.  hf.,  Cowles  well,  -    124 

19,  (est.),                     -  -    222 
Scott.    T.  24,  R.  21  E. 

Top  of  Mayville  beds,  -      7( 

Sec.  12,  Outcrop,  Cincinnati,      -  7c 

24,E.hf.,  -    168 
Sevastopol.    T.  28,  R.  26  E. 

Racine  limestone  near  Whitefish  bay,  3 
Sandbank,  R.  27,  E.,  Whitefish  bay,    1 

Sec.  10,  S.  W.  qr.,  gen.  level,  -    127 

18,  S.  Hne,  80 

20,  bank,  -    193 

21,  N.  E.  qr.,        -            -  133 

27,  S.  W.  qr.  (est.),  ridge,  100 

28,  mid.  E.  Hne,  -    116 

28,  S.  E.  qr.,  stream,        -  56 

29,  N.  E.  qr.,       -        -  -    155 
33,  S.  E.  qr.,  hill,  62 

Sheboygan.    T.  15,  R.  23  E. 

Sheboygan  post-office,  53 
Sheboygan  and  Fond  du  Lac  R.  R. 

station,  -        5 

Lake  Shore  R.  R.  station,        -  7 

Lighthouse  point,  bank  of  lake,  -      46 

Sec.   4,  near  N.  E.  corner  R.  R.,  60 

4.  mid.  N.  line,     -  85 

6,  mid.  S.  Hne,  Sheboygan  riv.,    74 

6,  S.  E.  corner,  highland,  -     149 

7,  center,  N.  hf.,  Rabe's  quarry,  73 
9,  S.  E.  qr.,  Roth's  quarry,  -      17 

River  opposite  quarry,  13 

Sec.  10,  near  center,  -      55 

10,  near  center,  R.  R.  crossing,      46 

10,  Pigeon  river  above  dam,  -      16 
16,  N.  hf.,  rising  to  W.,  25 
16,  mid.  S.  Hne,    -  126 
21,  near  center,  highland,  -     127 

30,  N.  E.  qr.,  gen.  level,  111 

33,  S.  E.  qr.  of  S.  E.  qr.,  -      58 

34,  mid.  N.  W.  qr.,  62 

Sheboygan  Falls.    T.  15,  R.  22  E. 

Decca  Station,  179 

Sheboygan  Falls  Station,    -  -      85 

School  house,  118 

Sec.    2,  mid.  W.  Hne  N.  W.  qr.,  202 

11,  N.  E.  corner,  -  199 

12,  mid.  E.  Hne  S.  E.  qr.,  122 
18,  S.  W.  corner,  -     190 
21,  near  center,  saw  mill,  139 
24,  N.  E.  corner,  -    116 
27,  mid.     E.    Hne  S.    E.   qr., 

stream,        -  93 

27,  near  center,  hill,     -  -    159 

35,  S.  W.  qr.,  R.  R.  crossing,         96 


Sherman.  T.  13,  R.  21  E.  —  (con.)  Feet. 
Sec.  25,  quarter    mile    from  White 

Cedar  swamp,    -  -    473 

27,  W.  hf.,  highland.  -    339 
34,  N.  W.  corner,  (est,),   -  218 

Shields.    T.  9,  R.  14  E. 

Sec.  32,  quarry,       -  -    214 
Somers.    T.  2,  R.  22  E. 

Sec.    1,  mid.  S.  hne  S.  E.  qr.,  44 

3,  S.  W.  qr.,  Pike  river,  -    30 

4,  mid.  N.  line,  R.  R.,    -  131 
4,  mid.  S.  line.  R.  R.,  -     124 
9,  mid.  S.  line,  R.  R.,     -  118 

10,  mid.  E.  line,  -      80 

16,  mid.  S.  line,  R.  R.,     -  103 

21,  mid.  S.  line,  R.  R.,  -     109 

28,  mid.  S.  hne,                -  101 
34,  center,        -  -     129 

Somers.    T.  2,  R.  23  E. 

Kenosha  Station,         -           -  40 

Sec.    5,  S.  W.  corner,  50 

7,  S.  line,  R.  R.,        -  -      35 

18,  S.  line,  R.  R.,  50 

19,  center,  R.  R.,  45 

19,  S.  line,  R.  R.,        -  -      40 
Spring  Prairie.    T.  3,  R.  18  E. 

Smith's  quarry,       -  -     188 

Sec.   5,  S.  W.  qr.,  highland,  -  401 

7  and  8,  average,       -  -    340 

8,  S.  W.  qr.,        -  231 
17  and  18,  average,     -  -    370 

20,  mid.  W.  Hne,  352 

26,  E.  hf,  -    201 

27,  S.  W.  comer,  stream,  284 

29,  center,        -  -    382 
34,  N.  W.  qr.,  stream,      -  245 

Spring  Valley.    T.  2,  R.  10  E. 

Orford  Station,        -  -    313 

Sec.  2,  mid.  E.  line,  -    350 

3,  N.  Hne  of  N.  E.  qr.,  -  418 

3,  S.  E.  qr.,    -  -     334 

3,  S.  W.  qr.  of  S.  W.  qr.,  314 

4,  N.  W.  qr.,  stream,  -    291 
4,                                    -  338 
4,  S.  W.  qr.,  flat,       -  -    253 
4,  S.  E.  qr.  of  S.  E.  qr.,  852 

9,  center,        -  -    321 
11,  N.  E.  qr.,        -            -  423 
11,  S.  W.  qr.,              -  -    342 

11,  hill,      -    '  396 

12,  center  N.  hf.,        -  -    389 
12,  S.  E.  qr.,  flat.  283 

12,  outcrop,      -            -  -    301 

13,  mid.  N.  line.  -           -  300 
15,  S.  E.  qr.,    - '  -    321 

17,  S.  E.  qr.,  stream,        -  215 

18,  S.  W.  qr.,  Taylor's  Creek,      204 

19,  N.  W.  corner,        -  -     220 

21,  N.  E.  qr.  of  N.  W.  qr.,  R.  R.  236 
24,  E.  Hne  of  S.  E.  qr.,  -    405 

28,  N.  E.  qr.,        -            -  296 

33,  S.  E.  qr.,   -  -     268 

34,  N.   W.  qr.,   Galena   Hrne- 

stone,     -  -    345 

34,  N.  W.  qr.,  summit,     -  394 


TOPOGRAPHY. 


125 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Spring  Valley.  T.21,  R.13E.— (con.)  Feet. 

Sec.  34,  S.  line  S.  W.  qr.,  -    336 
Stockbridge.    T.  19,  R.  19  E. 

Fork  in  roads  going  to  Chilton  and 

Sherwood,  -    397 
Three  miles  N.  of  Stockbridge  vil- 
lage,       -  -    388 
Two  miles  N.  of  Stockbridge  village,  383 
One  and  a  half  miles  N.  of  Stock- 
bridge  village,    -  -    358 
Four  corners  N.  of  Stockbridge  vil- 
lage,      -  -    214 
Stockbridge  village,     -  231 
Sec.  28,  mid.  N.  line  N.  W.  qr.,  399 

Sturgeon  Bay.    T.  27,  R.  26  E. 
Top  of  hill  N.  of  Sturgeon  Bay  vil- 
lage, -     113 
Sec.  5,  junction  Racine  and  Coral 

beds,                       -  58 

5,  top  of  rock,            -  -      75 

5,  valley,             -           -  44 

9,  E.  hi,  ridge,          -  -      62 

•  9,  S.  W.  qr.,  top  of  rock,  44 

9,  S.  E.  qr.,  top  of  rock,  -      61 

Sugar  Creek.    T.  3.  R.  16  E. 

Sec.    4,  S.  W.  qr.  W.  line,  -    353 

5,  Holden's  Lake,            -  325 

5,  mid.  N.  line,          -  -    367 

9,  near  center,                 -  340 

23,  N.  W.  corner,  creek,  -    312 

36,  mid.  N.  line,  -    420 

36,                        -           -  460 

Summit.    T.  7,  R.  17  E. 

Silver  Lake,                        -  -    278 

Nemahbin,       -                        -  289 

Sumner.    T.  5,  R.  13  E. 

Lake  Koshkonong,  -     184 

Sec.    7,  center  S.  hf,  creek,     -  188 

18,  near  center,  -     228 

Taycheedah.    T.  16,  R.  18  E. 

Lake  Winnebago,   -  -    162 

Sec.  5,  mid.  N.  line  N.  W.  qr.,  305 

5,  centre,        -  -    386 

22,  S.  W.  comer,  hill,      -  450 

22,  mid.  N.  line,  -    438 

25,  N.  line,  hills,  -            -  408 

25,  N.  line,  valleys,      -  -    358 

29,  S.  W.  qr.  of  S.  E.  qr.,  341 

32,  N.  W.  qr.,  R.  R.,  -  -    219 

Trenton.    T.  11,  R.  20  E. 

Newburg,  outcrop  on  river,  -    225 

Sec.   6,  mid.  E.  line,   -  314 

12,  mid.  S.  line,           -  -    342 

14,(?)hill,             -            -  345 

25,  N.  W.  qr.,              -  -    299 

Troy.    T.  4,  R.  17  E. 

Sec.  2,  N.  W.  comer,         -  -    253 

10,  S.  E.  corner,  R.  R.,     -  317 
1.1,  E.  hf.  center,  -    313 

11,  S.W.  qr.,  Castleman's  quarry,  233 
15,  S.  E.  qr.,    -           -  -    295 
22,  R.  R.  crossing,  300 
27,  centre  N.  hf..  stream,  -    273 

33,  mid.  S.  line,  hill,         -  310 


Turtle.    T.  1,  R.  13  E.  Feet. 

Crest  of  hill  E.  of  Beloit,     -  -    405 

Sec.  5,  level  Rock  prairie,  -           217 

9,  N.  E.  qr.,  -            -  -    227 

9,  N.  W.  qr.  of  S.  E.  qr.,  225 

13,  S.  E.  qr.,    -            -  -    330 

13,  mid.  S.  line  S.  W.  qr.,  306 

15,  N.  E.  corner,  -  222 

16,  center,        -  -    223 
19,  center,  -            202 

21.  mid.  S.  line.           -  -    228 

22,  N.  W.  qr.,       -  -            270 
22,  N.  E.  qr.,  -            -  -    280 
22,  N.  hf.,  near  R.  R.  cut,  302 
22,  bottom  of  Galena  Exposure,  246 

22,  summit  of  hill,       -  -    276 

23,  N.  E.qr.,        -  -            280 

28,  mid.  E.  line,  -    325 

29,  near  center,     -  218 
31,  N.  E.  corner,          -  -    211 

31,  N.  of  center,   -  -           188 

32,  center  N.  hf.,         -  -    229 

33,  N.  E.  comer,  -  266 
Two  Rivers.    T.  20,  R.  24  E. 

Sec.  22,  N.  W.  qr.,  -      53 

River  at  Neshoto,        -  -             29 
R.  R.  crossing  near  Two  Rivers,    -      14 

Utica.    T.  17,  R.  15  E. 

Pickett's  station,    -  -    266 

Pickett's  quarry,          -  242 

McFarland's  quarry,           -  -    264 

Fisk's  corners,  -            259 

Flat  E.  of  Rush  Lake,        -  -    235 

Union.    T.  4,  R.  10  E. 

Evansville  station,  -  325 

Sec.   1,  N.  W.  corner,  -            321 

1,  N.  E.  qr.  of.  N.  E.  qr.,  mill.  238 

2,  N.  W.  corner,        -  -  '  336 
2,  N.  W.  qr.,      -  -            339 
2,  N.  W.  qr.,  stream,  -    288 

4,  N.  W.  qr.,      -  -            379 

5,  N.  E.  qr.,  -            -  -    379 

6,  N.  W.  comer,  R.  R.,  -           400 
6,  W.  hf.,  marsh,       -  -    377 

6,  S.  W.  comer,  -            427 

7,  N.  W.  qr.,              -  -    442 
10,  W.  hf.,  Union  village,  375 
12,  N.  W.  qr.,  hill,      -  -    412 

12,  near  center,    -  298 

13,  N.  W.  qr.,  stream,  -     293 

14,  center  E.  hi,  -  -            339 
18,  mid.  W.  line,  stream,  -    382 

18,  S.  W.  qr.,  flat,  -            368 

19,  S.  W.  qr.,               -  -     391 
19,  N.  W.  corner,  -            382 
22,  (est.)          -           -  -    407 
26,  S.  E.  qr.,        -  -            334 
26,  near  N.  E.  corner,  -    389 

29,  center  S.  hf.,  flat,  -            367 

30,  S.  E.  qr.,  well,       -  -    402 
30,  S.  W.  qr.,  valley,  -            345 

30,  near  center  W.  line,  -    336 

31,  N.  E.qr.,        -  »            383 
31,  N.  E.  qr.,  summit,  -    423 
31,  S.  W.  qr..        -  -            290 


126 


GEOLOGY  OF  EASTERN  WISCONSIN. 


LIST  OP  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  contln ued. 


Union.    T.  4,  R,  10  E.  —  (con.)  Feet. 

Sec.  33,  near  center  stream,  -    352 

34,  near  N.  W.  corner,     -  400 
Vernon.    T.  5,  R.  19  E. 

Fox  river  at  Big  Bend,  268 

Sec.  10,  mid.  E.  line,  -    359 

11,  N.  W.  corner,  369 

28,  valley,        -  -    291 
Washington.    T.  11,  R.  22  E. 

Highland  N.  of  Port  Washington,      108 

Top  of  bank  N.  of  Port  Washington,     115 

Hill  W.  of  Port  Washington,  -     159 

Port  Washington  station,        -  _  87 

Port  Washington,  beach  formation,      40 

Sec.  4,  N.  line,      ...    144 

9,  N.  line,                        *  157 

9^  center  N.  E.  qr.,    -  -     128 

9,  center,  172 

16,  N.  line,      -  -     127 

16,  Sauk  river,      -  87 

30,  center  S.  E.  qr.,     -  -    226 

32,  center,  108 

Waterford.    T.  4,  R.  19  E. 

Fox  river  above  dam  at  Waterford,     246 

General  level  E.  of  Waterford,  -    265 

Sec.  6,  N.  line,  330 

28.,  Vernon  valley,       -  -    291 

36,  mid.  N.  line,  -  211 

Waterloo.    T.  8,  R.  13  E. 

Waterloo  Station,  -            -  -    241 

Sec.   3,  S.  W.  qr.,      -             -  237 

5,  N.  W.  qr.,  -    340 

6,  N.  E.  corner,  -            -  341 
9,  near  mid.  N.  line,  -  -    222 
9,  mid.  N.  line,  R.  R.,    -  217 
9,  center,  creek,  -    209 

11,  near  center  S.  W.  qr.,    -  211 

16,  N.  W.  qr.,  marsh,  -    275 

17,  center  W.  hf.,  hill,      -  329 

17,  center,  marsh,        -  -    218 

18,  N.  W.  comer,  297 

19,  S.  E.  corner,  -    279 

23,  center  S.  hf.,  hill,        -  401 

24,  Crawfish  marsh,     -  -    248 

25,  N.  E.  qr.,        -  300 
25,  near  center  E.  hf.,  -    260 
27,  S.  E.  qr.,  289 

29,  near  center,  creek,  -  -    220 

29,  E.  hf..     -        -  245 

30,  mid.  N.  line  N.  E.  qr.,  -    320 

31,  N.  W.  corner,            -  326 

31,  S.  W.  qr.  of  S.  W.  qr.,  -     350 

32,  near  center  S.  hf.,      -  310 
32,  mid.  E.  line  S.  E.  qr.,  -    322 

35,  S.  E.  qr.,        -  299 

35,  mid.  E.  line,  hill,     -  -    326 

36,  center,  266 
Watertown.    T.  8,  R.  15  E. 

Watertown  Junction,  -    243 

Sec.  21,  mid.  E.  line  S.  E.  qr.,  -  345 
Waukesha.    T.  6,  R,  19  E. 

Waukesha  Station,  -    225 

Waukesha  School  House,         -  243 
June,  of  Niagara  and  Racine,village  250 

Sec.  13,  mid.  N.  E.  qr.,  336 


Waukesha.    T.  6,  R.  19  E.  —  (con.)  Feet. 

Sec.  13,  mid.  E.  line,  hill,     -  -    298 

17,  N.  W.  qr.,  creek,        -  305 

Wanpnn.    T.  13,  R.  15  E. 

Waupun  Station,     -  -    314 

Horicon  marsh,    -  280 

Wauwatosa.    T.  7,  R.  21  E. 

Wauwatosa  Station,  -      73 

Sec.    1,  N.  line  N.  E.  qr.,     -  -      71 

1,  N.  line  N.  E.  qr.,  R.  R.,  72 

1,  mid.  N.  line,  -      80 

1,  N.  line  W.hf.  N.  W.  qr.,        69 

1,  center  N.  hf.  S.  W.  qr.,  -      83 

3,  N.  W.  corner,  123 

3,  mid.  W.  line,  -     121 

3,  S.  %  post,  W.  line  S.W.  qr.,  178 

3,  near  S.  W.  comer,  -    193 

3,  E.  line,  plank  road,     -  85 

4,  mid.  N.  line,  -    160 
4,  center  N.  E.  qr.,  167 
4,  mid.  W.  line,  -    161 
4,  center  N.  E.  qr.,  145 

4,  mid.  line,  Fond  du  Lac  Rd.,  167 

5,  mid.  N.  line,  -  142 
5,  N.  W.  corner,        -  -     150 

5,  mid.  W.  line  N.  W.  qr.,  140 

6,  N.  line,  river,  -    115 

7,  N.  line,  Menomonee  river,       104 
7,  N.  W.  corner,        -  -     159 

7,  mid.  W.  line,  174 

8,  mid.  N.  line  N.  E.  qr.,  -     155 
8,  mid.  N.  line,  -  161 
8,  mid.  N.  line  N.  W.  qr.,  -     122 

8,  N.  W.  corner,  163 

9,  mid.  N.  line  N.  E.  qr.,  -     172 
9,  mid.  N.  line,     -  203 
9,  N.  W.  corner,        -  -    169 

10,  mid.  N.  line,  -            -  157 

10,  N.  W.  corner,        -  -     186 

10,  mid.  W.  line,     -         -  217 

10,  plank  road,  W.  line,  -     199 

11,  mid.  N.  line,     -          -  118 

11,  N.  W.  corner,        -  -     136 

12,  N.  line,  R.  R.    -         -  80 
12,  mid.  N.  line  N.  W.  qr.,  -     110 

12,  N.  W.  corner,    -        -  104 

13,  mid.  N.  line,  -    114 
13,  N.  E.  qr.,  R.  R.  and  plank  r'd,  100 

13,  N.  W.  corner,        -  -     125 

14,  mid.  N.  line,     -  150 

14,  N.  W.  corner,        -  -    180 

15,  N.  line,  Fond  du  Lac  road      192 
15,  mid.  N.  line  W.  hf.  N.  E.  qr.,  186 
15,  mid.  N.  line,     -  206 
15,  mid.  N.  line  N.  W.  qr.,  -     199 
15,  N.  W.  corner,             -  174 

15,  mid.  W.  line,          -  -     176 

16,  mid.  N.  line,     -  174 

16,  N.  W.  corner,        -  -    164 

17,  N.  line,  river,             -  100 

17,  N.  W.  corner,        -  -     139 

18,  mid.  N.  line,    -  159 

18,  N.  W.  corner,     -        -  199 

19,  mid.  N.  line  N.  E.  qr.,  -     186 
19,  mid.  N.  line,     -  180 


'- ''"•/. 

'-.Vy,  'I/, 


PLATE,  VIA 


T  O  T»  O  Ci  R  AP1  H I  C  AL,   ^1 AP    OK    M;  1 1AVAT7  K  E  E    CO. 

Chn«  La pham. 


TOPOGRAPHY. 


127 


LIST  OF  ELEVATIONS  ABOVE  LAKE  MICHIGAN  —  continued. 


Wauwatosa.  T.  7,  R.  21  E.  — (con.)  Feet. 

Sec.  19,  mid.  N.  line  N.  W.  qr.,  -    207 

19,  N.  W.  corner,     -        -  228 

19,  mid.  W.  line  N.  W.  qr.,  -    218 

19,  mid.  W.  line,     -  202 

20,  N.  line,  river,  -      95 
20,  mid.  N.  line,      -        -  115 
20,  N.  W.  corner,  -     141 

20,  N.  line  S.  W.  qr.,  R.  R.,  115 

21,  mid.  N.  line  N.  E.  qr.,  -    132 
21,  mid.  N.  line,     -  143 
21,  mid.  N.  line  N.  W.  qr.,  -     1:34 
21,  N.  W.  corner,  -            -  119 
21,  W.  line,  R.  R.,      -  -     100 

21,  mid.  line,  R.  R.,  80 

22,  mid.  N.  line,     -              -  134 
22,  mid.  N.  line  N.  W.  qr.,  -    166 
22,  N.  W.  corner,     -         -  201 
22,  mid.  W.  line,         -  -     1:34 

22,  near  center  S.W.  qr.,  pl.road,  141 

23,  N.  line  N.  E.  qr.,  plank  r'd,  148 
23,  mid.  N.  line,  -    169 
23,  mid.  N.  line,  N.  W.  qr..  179 
23,  N.  W.  corner,        -  -     150 

23,  W.  line  on  Holston  road,  115 

24,  N.  W.  corner,  -    140 
24,  W.  line  N.  W.  qr.,  plank  r'd,  136 
24,  W.  line  S.  W.  qr.,  Wauwa- 
tosa road,        -     "  -  -     120 

24,  W.  line  N.E.  qr.,  Lisbon  r'd,  123 

24,  R.  R.,  Lisbon  plankroad,  104 

26,  center  S.  E.  qr.,  94 

26,  W.  line  N.  E.  qr.,  -      43 

27,  N.  line,  R.  R.,  64 

27,  E.  line,  Spring  road,  -     116 

28,  W.  line,  Spring  road,  172 
28,  mid.  line,  Spring  road,  -     113 
28,  mid.  N.  line,  -  107 

28,  center  S.  E.  qr.,     -  -      90 

29,  W.  line,  Spring  road,  207 

29,  mid.  line,  Spring  road,  -     195 

30,  mid.  line,  Spring  road,  226 

30,  center  S.  W.  qr.,  R.  R.,  -     163 

31,  center,  175 

32,  W.  line,  R.  R.,      -  -     161 

32,  center,  R.  R.,  195 

33,  W.  line,  R.  R,,      -  -     169 

34,  W.  line,  R.  R.,  125 
34,  center,  R.  R.,        -  -     144 

Wayne.    T.  12,  R.  18  E. 

Kohlsville,  river,     -  -    409 

Sec,  34,  mid.  S.  line  S.  E.  qr.,  590 

36,  knoll,          -            -  -    517 

36,  mid.  S.  line  S.  W.  qr.,  511 

West  Bend.    T.  11,  R.  19  E. 

Barton  village,  S.  side,  -    461 

West  Bend  Station,     -  314 

Sec.    2,  mid.  S.  line  S.  W.  qr.,  -    461 

5,  W.  line  N.  W.  qr..     -  505 

10,  N.  E.  qr.,  -            -  -    353 

14,  N.  line  N.  W.  qr.,      -  330 

17,  mid.  N.  line,  -    517 

18,  mid.  N.  line  N.  E.  qr.,  564 
Westford.    T.  12,  R.  13  E. 

Head  of  Beaver  Lake,        -  -    282 


Westford.    T.  12,  R.  13  E.  —  (con.)   Feet. 

Sec.    1,  S.  E.  qr.,         -  314 

6,  S.  line  S.  W.  qr.,  -  -     372 

7,  S.  line  S.  W.  qr.,        -  375 
19,  center  S.  E.  qr.,     -  -    298 
19,  N.  W.  qr.,  stream,      -  412 
25,  near  center,  -    330 

25,  -                        -  276 

26,  and  W.  marsh,      -  -    292 

30,  near  N.  line  N.  W.  qr.,  378 

31,  N.  line  N.  W.  qr.,    '  382 
31,  near  center  E.  hf.,  hill,  -    412 

34,  S.  E.  qr.,         -  327 
Wheatland.    T.  2,  R.  19  E. 

Sec.  29,  mid.  E.  hf.,  -    200 

29,  near  S.  W.  corner,     -  270 
31,  near  S.  E.  comer,  -  -    280 

Wheatland.    T.  1,  R.  19  E. 

Sec.   4,  general  level,  -    231 

6,  S.  E.  corner,    -  287 

7,  S.  E.  corner,  -     268 
Whitewater.    T.  4,  R.  15  E. 

Whitewater  Station,  -    241 

Whitewater  Normal  Hill,        -  307 

Whitewater  creek,  -    228 

Whitewater  lake,        -  317 

Sec.   2,  S.  E.  qr.,    -  -    242 

2,  S.  W.  qr.,       -            -  259 

<  E.  hf.,        -            -  -    249 

4,  W.  hf.,           -           -  232 

19,  N.  hf.,        -            -  -    297 
Wilson.    T.  14,  R..22E. 

Sec.  5,  S.  line  S.  E.  qr.,  R.  R.  cross'g,  115 

5,  near  N.  line  R.  R.,     -  133 

6,  N.  W.  corner,  general  level,  131 
6,  mid.  N.  line,  kettles,  -  114 

8,  N.  line  R.  R.,        -  -     115 
17,  N.  line,  R.  R.,           -  105 

20,  N.  line,  R.  R.,       -  -    102 

30,  N.  line,  R.  R.,  109 

31,  N.  line,  R.  R.,       -  -     102 
Woodville.    T.  20,  R.  19  E. 

Dundas  Station,      -  -     160 

Stream  3  miles  E.  of  Sherwood,  256 
R.  R.  crossing  2%  m.  E.  of  Sherwood,  252 

Highland  E.  of  Sherwood,       -  318 
Wrightstown. 

Ledge,         -  -    240 

Wrightstown  village,  -  35 
Sec.    1,  S.  E.  qr.,  highland,  T.  21, 

R.  20,  -    331 

8,  mid.  S.  line  T.  21,  R.  20,  -    154 

35,  mid.  N.  line  T.  22,  R,  20,       332 
35,  mid.  E.  line  T.  22,  R.  20,  292 
35,  S.  E.  qr..  swamp,  T.  22,  R.20,  284 

Yorkville.    T.  3,  R.  21  E. 

Sec.  10,  S.  W.  corner,  Root  river,  -     128 

11,  S.  W.  corner,  188 

11,  mid.  S.  line,  branch  Root  R.,  155 

12,  S.  W.  qr.,  Ives  Grove,  204 

26,  N.  E.  qr.,  -  -    207 

27,  N.  E.  qr.,        -  177 

28,  mid.  E.  hf.,  -    137 

29,  S.  E.  qr.,         -  l(ly 

30,  Union  Grove,  -     102 


128  GEOLOGY  OF  EASTERN  WISCONSIN. 


OHAPTEE  II 
HYDKOLOGY. 

Drainage.  On  the  average,  about  165,512,000,000  barrels  of  water 
fall  annually  upon  the  district  under  discussion.  Of  this,  about  one- 
half  is  lost  by  evaporation  and  absorption,  and  the  remainder  runs 
away,  constituting  the  drainage  of  the  district.  Were  the  slope  of 
the  surface  much  increased,  the  water  would  be  discharged  so  rapidly 
as  to  do  much  permanent  damage  by  erosion  and  the  rapid  removal  of 
our  fertile  soil.  "Were  its  inclination  much  less,  the  drainage  would 
be  imperfect,  and  our  noble  water  powers  destroyed.  In  the  golden 
mean  presented,  a  mutual  adaptation  to  the  twin  industries,  agricul- 
ture and  manufacture  is  fortunately  secured.  The  drainage  of  the 
region  forms  part  of  two  great  systems,  the  Mississippi  and  the  St. 
Lawrence.  Perhaps  one-fourth  belongs  to  the  former  and  the  remain- 
der to  the  latter. 

The  watershed  between  these  systems  is  very  peculiar.  On  the 
Illinois  line,  the  divide  is  within  three  and  one-half  miles  of  Lake 
Michigan,  and  is  only  160  feet  above  that  body  of  water,  while  the 
surface  to  the  west  continues  to  rise  by  undulations  to  400  feet  and 
upwards.  A  little  north  of  the  state  line,  several  of  the  streams,  no- 
tably the  White  river,  the  outlet  of  Lake  Geneva,  flow  to  the  north- 
east, and  yet  reach  the  Mississippi. 

From  the  state  boundary,  the  line  of  the  watershed  pursues  a  north- 
westerly course,  becoming  more  and  more  elevated  till  it  passes  the 
Kettle  range  at  about  500  feet  above  Lake  Michigan,  whence  it  con- 
tinues still  to  the  northwest  till  it  suddenly  drops  200  feet  into  the 
Green  Bay  and  Eock  river  valley,  whence  it  curves  more  to  the  west, 
until,  on  the  highlands  of  Metomen,  at  about  400  feet  elevation,  it 
turns  abruptly  southward,  giving  rise  to  another  anomaly.  The 
streams  that  here  flow  east  discharge  into  the  Mississippi,  while  those 
that  flow  west  empty  into  Lake  Michigan.  Following  the  watershed 
onward  from  this  point,  it  gradually  curves  to  the  westward,  descend- 
ing to  the  portage  between  the  Fox  and  Wisconsin  rivers,  where  its 
elevation  is  little  more  than  200  feet.  From  thence  it  pursues  a 


HYDROLOGY.  129 

northward  course  to  the  highlands  of  Michigan.  A  section  along  the 
line  of  the  watershed  across  the  Green  Bay  and  Rock  river  valley, 
would  exhibit  its  peculiarities  almost  as  conspicuously  as  if  taken  at 
any  other  point,  and  so,  to  almost  the  same  extent,  would  a  projection 
of  the  whole  line  exhibit  the  valleys,  slopes  and  ridges  that  constitute 
the  salient  topographical  features  already  described.  It  is  evident 
then,  that  the  present  drainage  systems  are  not  the  cause  of  these 
features. 

At  some  points  the  elevation  constituting  the  watershed  is  so  slight 
as  to  be  scarcely  perceptible.  A  notable  example  of  this  is  found  in. 
Racine  county,  in  the  relations  of  the  head  waters  of  the  Eau  Pleine 
river,  a  tributary  of  the  Mississippi,  and  those  of  the  Root  river  that 
flow  into  Lake  Michigan.  Both  have  their  rise  in  an  extended  marshy 
valley,  so  nearly  level  that  it  is  at  times  very  difficult  to  determine 
which  way  the  water  flows.  On  the  county  and  state  maps  the  divide 
is  placed  seven  miles  from  the  point  where  it  was  at  the  time  of  my 
visit. 

The  Mississippi  basin  is  represented  in  the  district  by  the  Rock 
river  system,  comprising  that  river  and  its  tributaries,  and  the  Illinois 
river  system,  embracing  the  (Illinois)  Fox  river  and  the  Eau  Pleine 
river,  with  their  branches. 

The  St.  Lawrence  basin  includes  the  Lake  Michigan  system,  of 
which  the  principal  streams  are  the  Root,  Milwaukee,  Sheboygan, 
Manitowoc,  Twin,  Kewaunee  and  Ahnapee  rivers,  and  the  Green  Bay 
system,  to  which  the  important  Fox,  Wolf,  Oconto,  Peshtigo  and  Me- 
nomonee  rivers,  with  several  minor  streams,  belong. 

A  moment's  attention  to  the  courses  of  these  streams  reveals  many 
striking  peculiarities,  for  most  of  which,  upon  careful  study,  there  is 
an  obvious  cause.  Some  of  these  are  worthy  of  special  attention,  not 
only  from  the  inherent  interest  which  they  possess,  but  because  they 
illustrate  the  dependence  of  such  important  features  as  rivers,  which 
often  determine  the  location  and  relations  of  great  business  centers, 
upon  surface  geology. 

Beginning  at  the  south,  the  streams  of  Walworth  and  adjacent 
counties  on  the  east  first  claim  attention,  and  form  an  interesting 
group,  most  conspicuous  among  which  are  White  river,  Sugar  creek 
and  Honey  creek.  These  streams  all  flow  in  an  easterly  or  northeast- 
erly direction  for  a  distance,  and  then  abruptly  turn  south,  uniting 
with  each  other,  and  at  last  joining  the  Fox  river,  which  continues 
south  until  it  unites  with  the  Illinois  river,  through  which  its  waters 
finally  discharge  into  the  Mississippi  and  the  Gulf.  All  the  group 
occupy  deep  parallel  valleys  in  the  upper  part  of  their  course,  and  it 
Wia.  SUB.  — 9 


130  GEOLOGY  OF  EASTERN  WISCONSIN. 

is  only  when  they  debouch  into  the  lowlands  of  the  Fox  river  that 
they  turn  southward. 

The  contour  of  the  adjacent  country  forbids  the  supposition  that 
these  valleys  were  excavated  by  simple  drainage  erosion.  Their  di- 
rection corresponds  to  that  of  the  drift  movement  to  which  they  are 
undoubtedly  due.  They  bear  the  distinctive  marks  of  troughs,  up 
which  the  ice  mass  moved  from  the  northeast,  as  will  be  explained 
subsequently.  On  either  hand  there  are  vast  accumulations  of  drift, 
heaped  up  in  the  form  of  an  irregular  moraine,  or  of  rounded  hills  and 
parallel  ridges.  When  the  streams  reach  the  lower  land,  they  follow 
southward  along  the  foot  of  the  drift  hills,  in  what  was  formerly,  to 
some  extent  at  least,  the  bed  of  an  elongated  lake. 

It  is  noticeable,  also,  that  the  numerous  beautiful  lakes  of  this  re- 
gion fall  into  line  along  these  glacial  valleys,  and  owe  their  existence 
to  the  same  general  cause. 

The  Pike  river  in  Kenosha  county  is  but  an  insignificant  stream, 
but  its  course  is  very  instructive.  In  the  upper  portion  it  flows  in  a 
meandering  manner  toward  the  lake  in  the  direction  of  the  general 
slope  of  the  surface.  But  when  within  about  one  mile  of  the  lake 
shore,  it  turns  abruptly  southward  and  runs  parallel  to  it  for  about 
four  miles.  It  formerly  extended  farther,  but  the  encroachment  of 
Lake  Michigan  cut  across  the  narrow  tongue  of  clay  that  separated 
the  river  from  it  at  one  of  the  bends  just  above  Kenosha,  and  allowed 
the  stream  to  discharge  at  that  point.  But  the  old  gorge  reenters  the 
shore  bluff  farther  down  and  again  joins  the  lake  at  Kenosha  harbor. 
Drs.  Lapham  and  Hoy  have  both  previously  called  attention  to  this 
interesting  instance  of  lake  encroachment. 

At  the  point  where  the  stream  now  discharges,  a  sand  bar  is  formed 
which  turns  it  southward.  With  a  single  unimportant  exception,  all 
the  streams,  great  and  small,  along  the  Wisconsin  shore  of  the  lake, 
so  far  as  they  have  come  under  my  observation,  are  turned  to  the 
southward,  in  a  similar  way,  by  an  accumulating  bar  at  the  mouth. 
This  fact  has  heretofore  been  remarked  by  several  observers. 

It  is  noticed  also  that  where  piers  are  extended  into  the  lake,  the 
sand  rapidly  accumulates  on  the  north  side,  forming  "made  land," 
while  that  which  collects  on  the  south  side  is  inconsiderable. 

These  facts  show  clearly  that  the  drift  along  the  present  shore  is  to 
the  southward  and  would  seem  to  warrant  us  in  saying  that  there  is  a 
southward  lake  current  along  the  Wisconsin  shore.  This  furnishes 
the  key  to  the  explanation  of  the  course  of  the  Pike  river.  Formerly 
the  lake  stood,  relatively  about  50  feet  higher  at  this  point  than  it  now 
does  and  extended  inland  beyond  the  position  of  this  portion  of  the 


HYDROLOGY. 

Pike  river,  and  left  its  record  in  a  low  beach  ridge.  The  Pike  river 
seems,  at  that  time,  to  have  discharged  directly  into  the  lake,  and  it 
would  appear  that  there  was  then  as  now,  a  southerly  current  which 
forced  the  stream  southward  by  the  formation  of  a  bar  and  gave  it 
its  present  course.  The  gorge  it  now  occupies,  it  has  since  cut  from' 
the  yielding  clays.  This  little  river  then  seems  to  teach  us  something 
of  the  past  history  of  Lake  Michigan,  and  since  the  present  shore  cur- 
rent is  believed  to  be  due  to  the  prevailing  direction  of  our  winds,  it 
perhaps  also  teaches  us  something  of  ancient  meteorology. 

The  course  of  the  Milwaukee  river  is  even  more  interesting.  It 
originates  chiefly  in  Fond  du  Lac  and  Sheboygan  counties  from  a 
number  of  nearly  parallel  southward-flowing  streams,  which  gradually 
unite  to  form  the  main  river.  At  West  Bend  it  turns  abruptly  east- 
ward. After  passing  Newburg  it  makes  a  rude  sigmoid  flexure  to 
the  north,  and  resumes  its  eastward  course.  When  within  about  nine 
miles  of  the  lake,  it  bends  suddenly  to  the  right  and  flows  almost  di- 
rectly south  parallel  to  the  lake  shore  for  more  than  30  miles,  being 
distant  from  it  at  some  points  in  its  course  less  than  two  miles.  It 
really  then  consists  of  three  portions:  the  south  ward-flowing  parallel 
branches,  the  eastward-flowing  portion,  and  the  main  trunk  flowing 
south  as  last  mentioned.  The  course  of  the  river  in  each  of  these 
three  parts  requires  a  different  explanation. 

The  parallel  branches  occupy  so  many  valleys  enclosed  by  the  ridges 
of  the  Kettle  Range  which  here  develops  a  more  than  usual  parallel- 
ism among  its  component  ridges.  At  the  occasional  breaks  in  these 
ridges,  the  streams  find  the  means  of  uniting. 

At  West  Bend,  where  by  taking  advantage  of  these  interruptions 
the  united  stream  has  reached  the  east  flank  of  the  Kettle  Range 
proper,  its  course  is  intercepted  by  an  east  and  west  valley,  attended 
with  "kettles"  and  serpentine  ridges,  and  corresponding  to  the  direc- 
tion of  drift  movement,  in  short,  a  glacial  valley.  This,  the  stream 
follows  to  the  vicinity  of  Newburg,  when  it  passes  across  to  a  parallel 
valley  on  the  north.  These  two  east  and  west,  valleys  are  entirely 
analogous  to  those  in  Walworth  county,  already  mentioned ;  indeed, 
they  belong  to  one  system  of  topographical  features,  occupying  more 
or  less  conspicuously  the  whole  territory  between  them,  and  due  to  the 
same  glacial  action. 

Near  the  great  bend,  in  the  town  of  Fredonia,  the  stream  reaches  an 
ancient  beach  line,  which  marks  the  shore  of  the  lake  at  the  time  of 
the  deposit  of  the  Lower  Red  Clay,  yet  to  be  described.  The  river 
follows  along  this  beach  line  to  its  mouth  at  Milwaukee.  The  con- 
clusion can  scarcely  be  avoided  then  that  it  owes  its  course  to  this  re- 


132  GEOLOGY  OF  EASTERN  WISCONSIN. 

lationship,  and  that  the  explanation  is  the  same  as  that  given  for  Pike 
river  —  and  that  the  same  inference  as  to  a  southward  lake  current  is 
justified. 

We  have  a  similar  phenomenon  in  connection  with  the  east  mem- 
ber of  Two  rivers,  or  the  East  Tivin  river,  which  marks,  though 
much  less  definitely,  the  western  limit  of  the  Upper  Red  Clay,  follow- 
ing in  a  similar  way  the  sandy  beach  deposit,  that  marked  the  shore 
line  of  the  lake  at  the  time  of  its  formation.  It  would  seem  then  that 
as  far  back  as  we  can  trace  the  history  of  the  lake,  by  these  means,  it 
has  had  a  southward-flowing  shore-current  along  the  Wisconsin  side. 

The  courses  of  several  other  streams  belonging  to  the  Lake  Michi- 
gan system  are  to  be  explained  in  a  similar  way. 

The  upper  portions  of  the  Wolf,  Oconto,  Peshtigo  and  Menomonee 
rivers  are  essentially  similar  to  each  other.  Rudely  parallel  among 
themselves,  they  flow  in  the  direction  of  the  general  inclination  of 
the  surface,  exhibiting  nothing  peculiar  while  they  are  passing  over 
the  region  of  the  granitic  and  other  Archaean  rocks,  but  after  en- 
tering upon  the  territory  underlaid  by  Paleozoic  formations,  their 
several  directions  become  exceptional. 

The  Oconto  river,  after  flowing  parallel  to  the  Wolf  for  thirty-five 
miles,  turns  at  a  right  angle  to  the  east,  and  flows  directly  to  Green 
Bay,  while  the  Wolf  river  continues  straight  on  its  course  for  thirty 
miles,  when  it  turns  with  equal  abruptness  to  the  west,  afterwards 
more  gradually  to  the  south,  and  then  east,  and  at  Lake  Winnebago 
its  current  is  reversed  and  flows  northward,  so  that  after  a  circuit  of 
about  140  miles,  it  reaches  the  mouth  of  the  Oconto  and  mingles  with 
its  waters,  which  have  only  traveled  thirty  miles  since  the  rivers  part- 
ed company. 

The  distance  between  the  Wolf  and  Oconto  where  this  divergence 
takes  place  is  only  about  twelve  miles,  more  than  half  of  which  is  oc- 
cupied by  Shawano  lake  and  its  outlet,  and  only  drift  accumulations 
of  no  very  considerable  magnitude  make  up  the  divide. 

The  'Menomonee  and  Peshtigo  rivers  make  similar  abrupt  changes 
in  their  direction. 

By  referring  to  the  map,  showing  the  geological  formations  of  this 
region,  the  explanation  of  these  anomalies  becomes  at  once  apparent. 
It  will  be  seen  that  the  boundaries  of  the  formations  are  zig-zag,  or 
step-like,  and  that  the  rivers  follow  the  softer  formations  along  the 
face  of  these  steps. 

The  Wolf  river,  from  Shawano  south,  follows  along  the  nearer  or 
more  remote  cliffs  of  the  Lower  Magnesian  limestone,  its  bed  lying  in 
the  soft  Potsdam  sandstone,  until  in  the  to\vn  of  Ellington,  along  the 


HYDROLOGY.  133 

line  of  an  apparent  fault,  the  limestone  is  brought  athwart  its  course, 
and  it  turns  to  the  west,  still  following  the  face  of  the  Lower  Magne- 
sian  cliffs,  until  they  turn  southward  in  the  town  of  Mukwa,  when  the 
river  curves  in  the  same  direction,  and  at  length  in  the  bed  of  Poy- 
gan  lake  and  the  basin  of  the  Fox  river,  it  finds  its  way  across  the 
obtrusive  formation.  Its  waters  then  reverse  their  course  and  flow 
back  along  the  face  of  the  projecting  cliffs  of  the  Xiagara  limestone 
for  a  hundred  miles,  when  Porte  des  Morts  allows  them  to  escape  into 
the  great  lake,  at  a  point  not  half  the  distance  from  their  source  that 
they  have  traveled. 

The  Oconto  river,  on  the  contrary,  on  encountering  the  resisting 
Lower  Magnesian  limestone,  turns  sharply  to  the  east  and  flows  along 
the  north  face  of  the  formation  for  some  distance,  when  it  forces  its 
way  across  it,  forming  the  beautiful  falls  of  the  Oconto,  and  keeps 
directly  on  its  course  to  the  bay.  The  falls  are  occasioned  by  a  soft 
shaly  stratum  near  the  middle  of  the  formation,  there  being  hard, 
heavy  bedded  layers  of  dolomite  above  and  below.  The  softer  stratum, 
being  more  easily  eroded,  permits  the  water  to  undermine  and  throw 
down  the  heavy  beds  above  it,  thus  keeping  the  face  of  the  cliff  verti- 
cal and  causing  the  falls  to  slowly  recede.  The  perpendicular  fall  is 
about  twenty-two  feet,  with  a  considerable  descent  upon  the  rapids 
above  and  below. 

The  deflection  of  the  Menomonee  river  to  the  eastward  (town  33, 
ranges  21  and  22  E.)  is  to  be  attributed  to  the  barrier  interposed  by 
the  same  formation,  though  in  this  instance  it  is  far  less  conspicuous, 
as  the  formation  does  not  immediately  adjoin  the  river  on  the  south, 
nor  does  it  anywhere  in  the  vicinity  project  in  mural  cliffs,  according 
to  its  habit,  to  the  southward.  Yet  its  influence  on  the  drift  accumu- 
lations is  apparent,  and  it  is  none  the  less  the  cause  of  this  deviation 
of  the  river  from  its  general  course.  At  Grand  Rapids  the  river 
crosses  the  formation,  the  rapids  being  due  to  the  same  cause  as  the 
falls  of  the  Oconto.  The  shaly  stratum  is  here  harder,  however,  and 
the  layers  above  less  massive,  making  the  resisting  power  of  the  two 
portions  less  different,  so  that  the  result  is  a  series  of  rapids  instead 
of  vertical  falls.  Immediately  on  passing  this  barrier,  the  beautiful 
river  recurves  to  the  south,  indeed  to  the  west  of  south,  and  follows 
the  horizon  of  the  St.  Peters  sandstone,  having  the  Trenton  limestone 
on  the  east,  until  within  about  eight  miles  of  its  mouth,  where  it 
crosses  the  latter  formation  by  a  succession  of  rapids.  It  is  true  that 
between  the  Grand  Rapids  and  those  last  mentioned,  neither  the  St. 
Peters  sandstone  nor  Trenton  limestone  appear  as  obvious  barriers, 
the  channel  of  the  stream  being  excavated  in  drift,  but  there  is  good 


134:  GEOLOGY  OF  EASTERN  WISCONSIN. 

reason  to  believe  that  the  original  surface  of  the  drift,  which  controlled 
the  direction  of  the  stream,  was  determined  by  these  underlying 
formations,  and  that  they  are  none  the  less  truly,  though  remote- 
ly, the  governing  influences.  This  view  of  the  case  is  supported  by 
the  unquestionable  facts  relating  to  the  similar  detour,  though 
in  an  opposite  direction,  of  the  Peshtigo  river  at  a  point  nearly  op- 
posite. 

Although  perhaps  more  than  usually  winding  in  its  minor  features, 
the  general  course  of  the  Peshtigo  river  is  exceptionally  direct,  and 
almost  exactly  southeast.  The  only  noteworthy  deviation  is  that  to 
which  attention  is  now  called.  From  the  outlet  of  Lake  l^oqueba,  its 
course  is  nearly  due  south  until  it  crosses  the  western  edge  of  the 
Lower  Magnesian  limestone  near  the  third  correction  line,  when  it 
immediately  sweeps  round  to  the  north  of  east,  and  flows  nearly  at 
right  angles  to  its  general  course  for  about  nine  miles,  approaching 
the  Menomonee  within  less  than  three  miles,  when  it  reverts  to  its 
southeastward  course. 

Throughout  this  northeasterly  course,  it  is  flanked  on  the  south- 
east by  a  wall  of  Trenton  limestone  and  St.  Peters  sandstone,  the  for- 
mer appearing  at  points  in  naked  ledges  left  projecting  by  the  disin- 
tegration of  the  latter.  The  present  bed  of  the  stream  is  excavated 
below  the  horizon  of  these  formations,  and  lies  in  a  trough  cut  from 
the  Lower  Magnesian  limestone,  for  the  greater  distance.  But  the 
dip  of  the  formations  to  the  eastward  is  greater  than  the  descent  of 
the  stream,  so  that  it  is  finally  enabled  to  surmo.unt  them  at  Potato 
and  White  rapids,  when  it  returns  to  its  original  direction. 

The  controlling  influence  of  this  barrier  is  also  shown  to  the  south- 
ward in  the  courses  of  the  "Little  river"  of  the  Peshtigo,  and  the 
"Little  river  "  of  the  Oconto. 

Perhaps  the  conjecture  may  be  ventured  that  the  Peshtigo  and  Me- 
nomonee rivers,  before  the  drift  period,  united  near  their  point  of 
nearest  approach  on  the  west  side  of  this  limestone  barrier,  and  passed 
it  through  a  common,  but  now  drift-filled  and  concealed,  channel,  for 
it  is  abundantly  evident  that  they  did  not  then  pass  it,  at  the  same 
points  they  now  do,  and  this  vicinity  appears  to  present  the  lowest 
point  to  which  the  western  edge  of  the  Trenton  limestone  is  depressed 
within  the  basin  of  these  rivers. 

On  the  flats  below  the  village  of  Peshtigo,  the  tortuous  course  of 
the  river  reminds  us  of  the  Asiatic  Meander. 

If  the  limitations  of  our  space  allowed  us  to  go  more  into  detail, 
and  to  examine  the  minor  streams,  we  should  find  equally  instructive, 
though  less  conspicuous,  phenomena.  "We  can  find  room  for  only  one 


HYDROLOGY.  135 

example,  that  of  the  East  Branch  of  the  Rock  river,  which  joins  the 
main  stream  in  Horicon  marsh. 

This  river  has  its  source  in  a  broad,  deep  valley,  extending  from  the 
southeast  to  the  northwest  (about  N.  30°  W.)  for  a  distance  of  up- 
wards of  20  miles.  In  the  towns  of  Wayne,  Theresa,  and  Lomira,  the 
width  is  from  one  to  two  miles  between  the  foot  of  the  hills  that  rise 
somewhat  abruptly  on  either  side.  The  valley  is  occupied  very  ex- 
tensively by  marsh.  Branches  from  the  north  and  south  unite  near 
the  center  and  form  the  main  stream,  which  taking  a  direction  nearly 
at  right  angles,  and  pursuing  a  serpentine  course  among  the  parallel 
north  and  south  ridges  of  this  region,  finally  discharges  its  waters 
into  Horicon  Marsh,  thus  forming  a  rude  italic  T,  the  upper  portion 
being  formed  by  the  branches  first  mentioned.  These  branches  are 
not  large,  nor  is  the  area  drained  by  them  considerable.  The  valley 
which  they  occupy  may  be  traced  onward  to  a  northward  connection 
with  the  valleys  crossing  the  ledge  in  Byron. 

It  is  scarcely  credible  that  this  valley  with  all  its  peculiarities  was 
due  to  the  unaided  erosion  of  the  streams  occupying  it.  Though  par- 
tially filled  with  drift  accumulations,  it  is  really  channeled  from  the 
Niagara  limestone,  which  distinguishes  it  from  the  class  last  under 
consideration,  where  the  essential  condition  was  two  formations  of 
different  resisting  power.  In  explaining  its  origin  we  must  again 
have  recourse  to  glacial  action.  We  find  that  the  drift  movement  was 
southward  along  the  axis  of  Lake  Winnebago,  but  on  surmounting 
the  ledge  on  the  east  and  south,  it  turned  somewhat  eastward  and  fol- 
lowed down  the  slope  of  the  surface  and  dip  of  the  rocks,  eroding  fur- 
rows that  have  a  southeasterly  trend.  One  of  these  is  the  valley  in 
question,  which  is  doubtless  more  extensive  and  well  defined  than  the 
adjoining  ones,  because  it  lies  south  of  Lake  Winnebago,  that  is,  more 
nearly  in  the  line  of  heavy  glacial  action.  The  angle  in  the  ledge  just 
north  of  it  doubtless  contributed  to  the  same  result. 

Relationship  of  some  of  the  streams  on  opposite  sides  of  the 
Kettle  Range.  One  further  feature  relating  to  certain  streams  and 
their  attendant  topography  deserves  notice.  It  consists  of  a  certain 
peculiar  and  definite  correlation  between  the  streams  on  the  east  and 
west  sides  of  the  great  dividing  drift  ridge. 

Where  an  extended  ridge-like  watershed  exists,  it  is  to  be  expected 
that  streams  on  the  opposite  sides  will  rise  near  each  other  and  flow 
in  opposite  directions,  at  right  angles  to  the  ridge,  but  in  the  present 
instance  they  are  arranged  in  pairs,  and  connected  across  the  summit 
by  more  or  less  well  defined  valleys,  so  that  the  relationship  cannot 
be  looked  upon  as  being  merely  fortuitous. 


136  GEOLOGY  OF  EASTERN  WISCONSIN. 

My  attention  was  first  called  to  those  in  "VValworth  county  some 
years  since  by  Dr.  II.  Hunt,  of  Beloit.  The  fluvial  pairs  and  the 
essential  facts  are  briefly  as  follows: 

/.  Geneva  Lake  and  Big  Foot  Prairie,  in  Walworth  county.  The 
bluffs  on  either  side  of  Geneva  Lake  rise  upwards  of  100  feet  above 
its  surface,  but  at  its  head  the  valley  extends  westward,  though  much 
narrowed,  and  joins  the  more  elevated  level  area,  known  as  Big  Foot 
prairie,  whose  present  drainage  is  southwestward,  the  watershed  being 
on  its  margin  next  Geneva  Lake,  and  less  than  two  miles  from  it. 
The  surface  is  more  elevated  on  either  side  of  the  prairie,  which  bears 
evidence  of  having  formerly  been  occupied  by  a  lake. 

2.  Delavan  Lake  and  the  White  river,  in  Walworth  county.  The 
valley  of  Delavan  Lake  is  very  similar  to  that  of  Lake  Geneva,  but 
it  lies  on  the  western  slope.  From  it  a  well  defined  valley  extends 
across  the  divide  and  connects  with  the  valley  of  White  river,  but  the 
elevation  of  the  summit  is  greater  than  in  the  previous  instance. 

j.  Turtle  creek  and  Sugar  creek,  in  Walworth  county.  The  head 
waters  of  Turtle  and  Sugar  creeks  are  connected  by  a  narrow  band  of 
marsh,  bordered  on  the  south  by  a  line  of  bluffs,  and  on  the  north  by 
a  more  gentle  ascent.  Its  whole  aspect  is  that  of  a  fluvial  flat. 

4.  The  Bark  and  Oconomowoc  rivers  and  the  branches  of  Cedar- 
creek,  in  Washington  county.     These  streams  constitute  a  double  pair, 
each  of  the  rivers  rising  in  a  marshy  valley  in  very  close  association 
with  the  headwaters  of  Cedar  creek,  the  elevations  separating  them 
being  very  slight. 

5.  Rubicon  river  and  the  northern  branch  of  Cedar  creek,  in 
Washington  county.     Between  Cedar  lake  and  the  headwaters  of  the 

Rubicon  river  lies  an  elongated  marsh,  occupying  a  notable  depression 
in  the  otherwise  elevated  ridge. 

These  facts  naturally  suggest  the  question,  Did  the  streams  on  the 
east  side  formerly  flow  across  the  present  summit,  or  was  the  reverse 
the  case;  or,  again,  are  these  facts  to  be  otherwise  explained?  In 
answer,  it  is  to  be  remarked,  in  the  first  place,  that  the  watershed  in 
question  is  either  formed  by,  or  is  closely  related  to,  the  great  drift 
ridge  previously  described,  and  that  this,  as  I  shall  hereafter  attempt 
to  demonstrate,  is  a  moraine,  formed  as  an  accumulation  along  the  foot 
of  an  immense  sheet  of  moving  ice.  If  this  can  be  clearly  pictured  to 
the  mind,  it  will  at  once  become  evident  that  the  waters  from  the  melt- 
ing ice  mass  must  find  their  way  across  the  accumulated  drift,  and  as 
the  amount  of  water  discharged  must  have  been  immense,  deep  valleys 
would  be  cut  at  intervals  of  no  great  distance.  This  is  probably  the  true 
explanation  of  the  initial  formation  of  these  valleys  across  the  summit. 


HYDROLOGY.  137 

Origin  and  Geological  Relations  of  the  Lakes  of  Eastern  Wis- 
consin. Analogous  to  the  topics  which  have  been  under  discussion, 
is  the  consideration  of  the  position  and  cause  of  the  numerous  lakes 
which  lend  their  attractions  to  the  beautiful  scenery  of  this  portion 
of  the  state. 

It  has  already  been  said  that  the  great  lake  on  the  east  lies  in  a 
basin  excavated  chiefly  from  the  soft  rocks  of  the  Devonian  age,  and 
that  its  western  edge  rests  upon  the  Upper  Silurian  limestone  along 
the  trend  of  which  it  lies.  The  fact  that  its  bottom  lies  three  hun- 
dred feet  below  the  level  of  the  ocean,  shows  that  it  could  not  have 
been  eroded  by  running  water  in  its  present  position;  and  its  width 
and  the  regular  contour  of  its  bottom  forbids  the  supposition,  even  if 
the  proper  elevation  and  slope  were  given  it.  The  drift  on  its  margin 
contains  material  that  there  is  every  reason  for  believing  came  from 
its  bed,  and  the  polishing  and  grooving  of  the  rocks  that  form  its 
rim  show  that  it  has  been  the  theatre  of  powerful  glacial  action,  and 
to  this  cause  its  present  regular  outline  and  great  depth  and  breadth 
are  undoubtedly  due.  That  it  may  have  been  deeply  channeled  by 
running  water  before  the  glacial  period,  and  that  such  channels  may 
have  had  a  directing  power  over  the  subsequent  and  more  powerful 
glacial  action  is  not  improbable.  The  fact  that  it  lies  within  seventy 
miles  —  less  than  its  own  breadth  —  of  a  region  where  the  drift  action 
was  very  slight,  and  the  preglacial  contour  of  the  surface  was  not 
more  than  slightly  modified,  a  region  whose  present  elevation  is  less 
than  three  hundred  feet  above  the  lake  surface,  and  beyond  which  the 
drift  shortly  disappears  entirely,  lends  support  to  this  view. 

Green  Bay,  Lake  Winnebago  and  the  former  Lake  Horicon  oc- 
cupy portions  of  a  similar  glacial  channel,  and  owe  their  origin  to 
slight  drift  obstructions  thrown  across  the  valley.  The  fact  that  Lake 
Winnebago  discharges  through  a  channel  having  a  rocky  bottom  does 
not  militate  against  this  statement,  for  the  real  channel  of  the  valley 
is  nearer  Clifton,  on  the  east  side  of  the  lake.  The  drift  blocks  this 
up,  and  the  lake  pours  over  a  low  rock  barrier  that  separates  it  from, 
the  parallel  valley  of  Butte  des  Morts,  which  occupies  a  lower  geolog- 
ical horizon. 

Were  the  drift  removed,  a  channel  between  Menasha  and  Clifton 
would,  without  question,  drain  the  lake. 

Lake  Horicon  was  originally  confined  by  drift,  which,  in  time,  by 
its  own  outflow,  was  cut  away.  Its  place  was  subsequently  supplied 
by  an  artificial  dam,  which  restored  the  lake.  This,  again,  was  re- 
moved, and  the  area  is  now  a  marsh. 

Lake  Poygan  seems  to  have  been  excavated  by  glacial  action. 


138  GEOLOGY  OF  EASTERN  WISCONSIN. 

chiefly  from  the  yielding  Potsdam  sandstone,  the  direction  of  drift 
movement  being  here  to  the  westward.  It  is  probable  that  a  river 
channel  existed  there  previously,  which  enabled  the  ice  to  act  with 
greater  efficiency. 

Green  Lake,  Puckawa  Lake  and  Rush  Lake  all  lie  in  one  valley 
along  which  the  glacier  plowed  its  way.  Hush  Lake  was  eroded  from 
the  soft  St.  Peters  sandstone,  having  the  harder  Lower  Magnesian 
limestone  for  its  bed,  while  the  Trenton  limestone  borders  it  on  the 
east.  The  rise  that  separates  this  from  Green  Lake  is  scarcely  per- 
ceptible. The  east  end  of  the  latter  lake  occupies  the  same  geological 
horizon,  but  the  dip  of  the  strata  is  such  at  this  point  that,  in  its 
length,  the  lake  cuts  across  the  Lower  Magnesian  limestone,  the  Mad- 
ison sandstone,  the  Mendota  limestone,  and  into  a  still  lower  division 
of  the  Potsdam  sandstone.  At  the  west  end  it  is  confined  by  a  range 
of  drift  hills  crossing  the  valley.  To  these  this  beautiful  lake  may  be 
said  to  owe  its  existence.  If  they  were  removed,  the  lake  would  dis- 
charge itself  into  Lake  Puckawa,  to  the  west,  its  elevation  being  the 
greater.  The  contour  of  these  hills  shows  their  morainic  character 
and  indicates  that  they  were  heaped  up  there  by  the  tongue  of  ice  that 
filled  and  in  part  eroded  the  valley. 

Lake  Puckawa  was  eroded  in  the  same  way,  but  from  still  lower 
strata.  On  its  south  side  there  rises  a  cluster  of  hills  of  Archaean 
rocks,  which,  by  their  hardness  and  powers  of  resistance,  may  have 
forced  the  ice  mass  to  more  deeply  erode  the  softer  -sandstone  repos- 
ing on  their  flanks. 

Lake  Shawano  lies  along  the  northern  base  of  an  east  and  west  line 
of  bluff's  capped  by  Lower  Magnesian  limestone  resting  upon  Potsdam 
sandstone,  from  which  the  basin  of  the  lake  has  been  excavated.  Its 
longer  axis  harmonizes  with  the  direction  of  glacial  movement,  which 
in  this  region  was  from  the  east  to  the  west.  "We  have,  then,  an 
easily  eroded  stratum,  adjacent  to  a  more  resisting  one,  with  a  com- 
petent eroding  agency  acting  in  a  favorable  direction,  resulting  in  the 
formation  of  Lake  Shawano. 

Lake  KosKkonong  likewise  lies  in  the  direction  of  glacial  progress 
and  is  due  to  the  ease  with  which  the  St.  Peters  sandstone  was  exca- 
vated. An  ancient  stream  had  probably  cut  down  to  and  perhaps 
through  it  —  for  such  is  the  fact  in  reference  to  the  preglacial  Rock 
river  channel  farther  south  —  and  the  ice  plow,  taking  advantage  of 
this,  furrowed  and  filled,  leaving  a  wide,  shallow  basin. 

The  foregoing  lakes,  it  will  be  noticed,  have  a  definite  relationship 
to  the  geological  formations  adjacent  and  subjacent  to  them,  and  are 
all  to  be  accounted  for  on  essentially  the  same  principle,  viz. :  The  un- 


HYDROLOGY.  139 

equal  hardness  of  the  strata  acted  upon  by  a  powerful  excavating 
agency,  that,  unlike'  rivers,  did  not  cany  away  its  rubbish  as  fast  as 
formed,  but  heaped  it  up  promiscuously  in  its  own  track  as  it  melted 
backward,  the  inevitable  result  being  the  formation  of  lakes  along  its 
abandoned  channels. 

The  number  originally  thus  formed  was  vastly  greater  than  the 
number  now  in  existence,  the  great  majority  having  cut  down  their 
own  barriers  and  drained  themselves. 

These  may  then  be  said  to  be  glacial  lakes,  for  there  is  no  reason 
to  suppose  that  any  one  of  those  described,  existed  before  the  drift 
period.  But  as  the  most  of  them  were  probably  represented  as  river 
valleys  or  gorges,  and  as  their  present  existence  is  due  also  to  the  un- 
equal powers  of  resistance  of  the  rock  formations,  this  class  of  lakes 
is  not  entitled  to  be  termed  glacial  lakes  in  the  same  sole-dependent 
sense  as  the  following,  the  most  of  which  show  little  or  no  relation- 
ship or  dependence  on  the  underlying  strata^  but  are  drift  lakes  in  an 
exclusive  sense. 

The  class  now  to  be  described  may  be  subdivided  into  two  subordi- 
nate ones.  The  first  are  those  which  lie  in  valleys,  whose  greatest  length 
is  in  a  line  with  the  glacial  grooves,  and  in  this  respect  are  like  the 
last  class,  differing  from  them  only  in  being  independent  of  the  strata 
beneath.  These  were  formed  in  drift  troughs  by  the  retreating 
glacier,  very  much  as  the  class  above  described  were,  only  the  troughs 
are  not  excavated  rock  channels,  but  valleys,  between  drift  ridges. 

The  other  kind  are  those  whose  greatest  length  lies  at  right  angles 
instead  of  parallel  to  the  glacial  grooves. 

These  lie  between  the  ridges  that  accumulated  at,  the  foot  of  the 
glacier  and  which  were  rudely  parallel  to  each  other,  yet  sometimes 
joining  mutually,  and  again  separating  to  a  considerable  interval,  they 
left  enclosed  hollows,  which  on  filling  with  water,  became  lakes. 

We  would  perhaps  be  justified  in  being  even  more  specific  than  we 
are  in  calling  these  drift  lakes,  by  designating  them  moraine  lakes. 

From  the  nature  of  the  case,  forms  intermediate  between  all  the 
foregoing  are  to  be  expected,  and  are  found  to  occur,  and  with  the  gen- 
eral explanations  given,  it  will  be  needless  to  designate  in  the  case  of 
each  of  the  numerous  small  lakes,  the  precise  method  of  formation, 
although  it  is,  in  most  cases,  sufficiently  clear. 

More  than  one  hundred  of  these  lakes  lie  along  or  adjacent  to  the 
Kettle  Kange,  and  form  an  important  element  of  its  picturesque 
scenery.  Among  the  most  noteworthy  are  Geneva,  Delavan,  Como, 
Turtle,  Bass,  Roldens,  Otter,  Silver,  Pleasant,  Green  and  the  Troy 
lakes  in  Walworth  county;  Mary,  Elizabeth,  Camp  and  Silver  lakes 


140  GEOLOGY  OP  EASTERN  WISCONSIN. 

in  Kenosha  county;  Wind,  Long  and  Browii/s  in  Racine  county; 
Muskego,  Pewaukee  and  that  beautiful  cluster  known  as  the  Ocono- 
mowoc  lakes,  about  forty  in  number,  in  Waukesha  county;  Cedar, 
Little  Cedar  and  Silver  lakes  in  Washington  county;  Long  and  Round 
lakes  in  Fond  du  Lac  county;  Elkhart  and  Bear  lakes  in  Sheboygan 
county,  and  Cedar,  Pigeon  and  Wilke  lakes  in  Manitowoc  county. 
Rock  lake  in  the  town  of  Lake  Mills,  Jefferson  county,  and  Clear  lake, 
near  Milton,  Rock  county,  belong  to  the  same  category,  though  un- 
connected with  the  main  chain  of  the  Kettle  Range. 

Of  the  foregoing,  Muskego,  Wind  and  several  smaller  lakes  asso- 
ciated with  these,  bear  evidence  of  having  formerly  constituted  parts 
of  a  much  more  extensive  body  of  water,  that  leveled  by  erosion  and 
deposition  the  original  uneven  surface  in  their  vicinity,  so  that  its 
primitive  drift  features  disappeared  and  with  them  the  corresponding 
features  of  those  lakes,  so  that  they  do  not  now  present  those  charac- 
teristics which  are  common  to  the  majority  of  the  others. 

There  is  also  some  evidence  that  the  comparatively  level  area  in 
which  the  Oconomowoc  lakes  are  embosomed  was,  immediately  after 
the  glacial  period,  occupied  by  an  extensive  lake  that  reduced  the  gen- 
eral surface  to  its  present  degree  of  uniformity  by  washing  down  pro- 
jecting points,  while  it  was  unable  to  fill  the  present  lake  basins,  they 
being  below  the  line  of  its  wave  action. 

Tlw  value  of  the  lakes  of  eastern  Wisconsin  is  much  greater  than 
is  sometimes  apprehended.  Beauty  is  not  an  unimportant  element  of 
value.  Attractive  scenery  adds  materially  to  the  worth  of  both  rural 
and  urban  property. 

The  wealth  of  eastern  Wisconsin  has  been  materially  increased  dur- 
ing the  last  decade,  simply  through  the  charm  of  its  beautiful  lakelets. 
Thousands  of  citizens  of  other  states  have  visited  them,  and  large  ho- 
tels and  beautiful  summer  residences  have  been  erected  as  substantial 
tokens  of  the  enduring  admiration  which  these  gems  of  nature  have 
awakened. 

The  salutary  influence  which  they  exert  over  the  people  of  our  own 
state  by  tempting  to  healthful  recreation  and  by  the  cultivation  of 
aesthetic  tastes  is  scarcely  to  be  estimated. 

To  those  who  admire  a  broad  expanse  of  water,  Lake  Winnebago, 
with  its  cliffs  on  the  one  hand  and  its  wooded  plains  on  the  other; 
Green  Bay,  with  its  rocky  battlements  on  the  right,  its  forests  on  the 
left,  its  viewless  limits  on  the  north,  its  islands  and  harbors,  and,  par 
excellence,  the  oceanic  Lake  Michigan  present  their  varied  attrac- 
tions. 

Among  the  smaller  lakes  that  have  been  accorded  the  greatest  meas- 


HYDROLOGY.  141 

ure  of  admiration,  attention  may  be  called  to  the  deep,  clear  waters 
and  wooded,  gravelly  shores  of  the  picturesque  Geneva,  the  charming 
variety  of  the  two  score  lakelets  of  the  Oconomowoc  cluster,  the  em- 
erald waters  and  picturesque  glens  and  cliffs  of  Green  Lake,  the  ro- 
mantic little  Elkhart,  a  gem  in  a  rustic  framework  of  wooded  drift 
knolls  and  kettles,  and  the  quiet,  restful  beauty  of  Rock,  Brown,  Clear 
and  Delavan  lakes.  Lakes  Koslikononq,  Pewaukee,  Puckawa  and 
others  are  favorites  with  sportsmen. 

These  lakes  abound  in  a  variety  of  excellent  fish,  and  are  the  resort 
of  large  numbers  of  water-fowl.  Through  the  labors  of  the  state  fish 
commissioners,  and  the  enlightened  and  generous  action  of  private 
citizens,  some  of  them  have  recently  been  stocked  \vith  choice  varie- 
ties of  fish  from  other  waters,  and  it  is  confidently  believed  that  they 
will,  under  a  continuance  of  this  enlightened  policy,  render  a  hand- 
some contribution  of  excellent  food  in  return. 

Their  value  as  water  power  reservoirs,  though  not  as  yet  appreci- 
ated, will,  in  the  unfoldings  of  the  resources  of  this  region  in  the 
future,  perhaps  surpass  both  the  considerations  above  mentioned. 
This  point  will  receive  brief  consideration  under  the  head  of  water 
power,  a  few  pages  in  advance. 

Water  Supply.  The  surface  soil  possesses,  on  the  average,  a  fair 
degree  of  absorptive  power,  and  the  underlying  strata,  both  of  the 
drift  and  rock  formations,  consist  of  alternating  pervious  or  impervi- 
ous layers,  thus  presenting  suitable  conditions  for  an  excellent  water 
supply.  A  less  absorptive  soil  would  cause  a  greater  proportion  of 
the  rainfall  to  be  lost  by  surface  drainage,  and  a  uniformly  porous  or 
uniformly  impervious  rock  structure  beneath  would  be  less  favorable 
to  frequent  springs  or  veins  of  water  that  could  be  reached  by  wells. 
As  it  is,  there  are  few  localities  at  which  an  abundant  supply  of  water 
cannot  be  reached  at  moderate  depths. 

Attention  will  here  be  chiefly  confined,  however,  to  the  natural 
sources  of  supply  provided  in  springs.  To  casual  observation  these 
appear  to  be  scattered  promiscuously  over  the  region,  without  any 
definite  geological  relations,  but  such  is  not  the  fact.  There  are  two 
general  systems  of  springs;  those  that  originate  in  the  drift  deposits, 
and  those  that  flow  from  the  rock.  The  springs  of  each  group  occu- 
py several  different  horizons,  which  it  will  be  interesting  to  notice 
briefly,  as  the  subject  is  one  of  great  importance.  It  is  estimated  by 
some  authorities  that  one-third  of  the  diseases  which  aiflict  mankind 
are  due  to  the  use  of  impure  water.  Though  this  estimate  may  be 
too  high,  it  is  abundantly  demonstrated  that  some  of  the  most  terrible 
diseases  are  directly  attributable  to  this  cause.  If  unaided  nature  has 


M2  GEOLOGY  OF  EASTERN  WISCONSIN. 

provided  us  any  means  of  escape  from  this  prolific  source  of  danger, 
it  is  quite  certain  to  be  found  in  our  deep  seated  springs. 

There  are  several  reasons  why  spring  water  is  more  likely  to  be 
pure  than  that  of  wells.  On  the  average  it  comes  from  greater  depths 
and  has  passed  through  a  greater  extent  of  the  deeper  strata  which 
are  comparatively  free  from  organic  impurities,  than  has  the  water 
of  wells,  which  is  usually  drawn  from  the  surface  of  the  water  level  be- 
neath the  location  of  the  wells.  Artesian  fountains  are  not  here  taken 
into  account.  The  water  of  wells  is  usually  stagnant,  while  that  of 
springs  is  active,  "  is  living  water." 

There  are  some  exceptions  to  the  first  part  of  this  statement.  Oc- 
casionally a  well  is  sunk  upon  an  active,  flowing,  underground  stream, 
in  which  case  the  superior  character  of  the  water  will  usually  be  very 
marked.  The  water  of  springs  is  not  liable  to  so  many  sources  of 
contamination,  and  they  more  readily  discharge  impurities  that  may 
find  their  way  into  them.  In  view  of  these  facts,  the  study  and  utili- 
zation of  the  numerous  springs  of  the  state  become  of  much  im- 
portance. So  far  as  possible  all  cities  should  be  supplied  by  water 
from  springs  or  Artesian  wells. 

The  lowest  noteworthy  horizon  from  which  springs  arise  is  the 
vicinity  of  the  junction  of  the  Potsdam  sandstone  and  the  Lower 
.Magnesian  limestone.  The  water  from  this  source  usually  has  a 
.temperature  of  48°  to  50°,  and  is  clear  and  comparatively  free  from 
organic  impurities,  but  contains  a  small  percentage  of  the  carbonates 
of  lime  and  magnesia,  and  in  some  cases  a  very  small  percentage  of 
iron,  with  usually  some  silica,  alumina  and  chloride  of  sodium.  But 
the  combined  amount  of  these  is  small,  and  the  water  is  "  soft,"  and 
very  pleasant  to  the  taste.  A  small  amount  of  free  carbonic  acid  is 
usually  present,  which  enhances  the  grateful  effect  of  the  water  upon 
the  palate  and  stomach.  The  springs  from  this  horizon  are  not  nu- 
merous. Mitchell's  spring  near  Berlin  is  a  fine  example,  and  deserves 
the  attention  of  the  people  of  that  place  as  a  source  of  pure  water  for 
domestic  purposes,  and  as  furnishing  favorable  conditions  for  trout 
raising.  Another  notable  spring  of  this  class  lies  near  the  road  be- 
tween New  London  and  Hortonville  (S.  W.  J  of  K  "W.  J  Sec.  28,  T. 
32,  R.  15  E.),  which  is  very  much  superior  to  the  water  from  the 
drift  wells  of  those  places. 

Above  this  horizon  springs  occur  but  rarely  till  we  reach  the  junc- 
tion of  the  St.  Peters  sandstone  with  the  Trenton  limestone.  Some 
shaly  impervious  layers  mark  this  division,  while  the  limestone  above 
is  fissured  and  the  sandstone  below  is  porous.  It  hence  follows  that 
the  springs  may  arise  either  above  or  below  the  impervious  stratum 


HYDROLOGY.  143 

according  to  circumstances.  (1)  Water  descending  from  above  may 
be  caught  and  carried  out  where  the  strata  are  cut  across  to  the  proper 
depth;  and  (2)  water  that  gained  access  to  the  sandstone  at  some  dis- 
tant and  more  elevated  point  may  rise  from  below  at  places  where  the 
confining  stratum  is  removed.  So  that  it  is  proper  to  include  in  this 
group  some  that  issue  from  ledges  somewhat  above  or  below  the  junc- 
tion of  the  formations.  These  springs  are  similar  in  general  character 
to  the  last,  but  usually  contain  a  more  considerable  percentage  of  the 
several  mineral  ingredients,  at  least  that  portion  of  them  that  are  de- 
rived from  the  limestone,  which  still  retains-  traces  of  many  of  the 
salts  that  we  have  reason  to  suppose  were  incorporated  with  it  when 
it  was  formed  beneath  the  ancient  ocean. 

To  this  class  belong  most  of  the  springs  that  issue  from  the  rock  in 
the  western  half  of  the  counties  of  Rock,  Jefferson,  Dodge  and  Fond 
du  Lao.  Though  differing  among  themselves,  they  are,  as  a  class,  of 
most  excellent  quality,  and  should  be  substituted  for  the  well  water 
of  those  regions,  so  far  as  practicable. 

A  number  of  springs  in  the  vicinity  of  Beaver  Dam  issue  from 
near  the  junction  of  the  Trenton  with  the  Galena  limestone;  and  at 
other  points,  streams  issue  from  the  latter  formation,  but  they  do  not 
seem  to  be  confined  to  any  single  stratum,  and  there  is  nothing  in  the 
nature  of  the  rock  to  ead  us  to  expect  any  well  marked  system. 

By  far  the  most  remarkable  water-bearing  horizon  is  found  at  the 
upper  surface  of  the  Cinninati  shales,  the  dividing  plane  between 
the  Upper  and  Lower  Silurian  formations.  The  upper  part  of  the 
shale  is  little  else  than  a  stiff,  compact,  blue  clay,  and  is  the  most  im- 
pervious stratum  in  this  portion  of  the  state.  Above  it  there  lies  a 
varying  thickness  of  fissured,  cavernous  Niagara  limestone,  through 
which  the  water  descends  till  its  progress  is  arrested  by  the  clay  from 
the  surface  of  which  it  flows  out  wherever  opportunity  offers.  Along 
the  east  side  of  the  Green  Bay  and  Rock  river  valley,  the  junction  of 
these  strata  is  exposed  at  frequent  intervals  for  one  hundred  and  fifty 
miles,  so  that  hundreds  if  not  thousands  of  springs,  great  and  small, 
mark  this  horizon.  When  a  heavy  mass  of  drift  clay  lies  against  the 
line  of  junction,  the  water  sometimes  issues  from  layers  of  the  lime- 
stone, several  feet  higher,  and  where  much  loose  rock  has  fallen  from 
the  cliffs  above,  the  stream  runs  in  a  concealed  channel  down  the 
slope,  and  appears  to  issue  scores  of  feet,  sometimes,  below  its  true 
point  of  exit  from  the  strata.  Yet,  notwithstanding  these  facts,  with 
proper  caution,  the  point  at  which  the  clay  and  limestone  join,  even 
when  concealed,  may  be  traced  approximately  by  this  line  of  springs. 

Many  of  these  fountains  are  very  large  and  strong;  indeed,  some 


GEOLOGY  OF  EASTERN  WISCONSIN. 

of  them  are  rather  to  be  conceived  as  streams,  issuing  from  the  rock 
full  fledged,  than  as  the  bubbling  source  of  a  rivulet,  implied  by  the 
term  spring.  In  some  places  they  furnish,  without  further  augmen- 
tation, sufficient  power  for  efficient  flouring  mills.  In  one  case  two 
mills  are  supplied  by  using  the  water  in  succession,  within  one-half 
mile  of  the  source. 

The  quality  of  the  water  of  this  class  varies  more  than  that  of  the 
preceding,  owing,  as  it  may  be  conjectured,  to  the  greater  or  less 
effect  of  the  shales  upon  it.  These  contain  organic  matter,  iron  py- 
rites, and  other  ingredients  which  on  exposure  indicate  their  unsta- 
ble chemical  nature,  by  changes  of  color  and  otherwise,  and,  by  so 
doing,  warrant  the  belief  that  they  sometimes  make  unfavorable  con- 
tributions to  the  stream  in  contact  with  them.  The  water  of  most  of 
them,  however,  is  clear,  cool  and  refreshing,  and  in  character  very 
similar  to  those  of  the  preceding  classes,  though'  somewhat  harder,  on 
the  average.  Several  are  supercharged  with  lime  salts,  which  are  de- 
posited as  travertine  about  the  spring,  on  the  escape  into  the  atmos- 
phere of  the  carbonic  acid  which  held  them  in  solution.  The  tem- 
perature is  also  varying,  being  dependent  of  course  upon  the  thick- 
ness of  the  limestone  above. 

Above  this  generous  horizon  there  is  no  well  marked  water-bear- 
ing stratum  of  rock,  although  there  are  numerous  fine  springs  issu- 
ing at  various  points  from  the  Niagara  limestone.  The  widely  known 
Waukesha  springs  are  examples.  Druecker's  spring,  near  Ozaukee, 
and  several  fine  ones  near  Sturgeon  Bay,  belong  to  a  similar  geologi- 
cal position. 

The  foregoing  are  all  derived  from  rocks  that  were  laid  down  under 
the  ancient  Silurian  ocean,  rocks  whose  ages  are  to  be  reckoned  by 
myriads  of  years,  and  from  which  there  has  at  least  been  a  liberal  al- 
lowance of  time  for  the  removal  of  whatever  soluble  matter  may  have 
been  originally  incorporated  in  them ;  and  yet  we  find  in  all  that  have 
been  analyzed,  varying  quantities  of  the  oceanic  salts.  The  remain- 
der issue  from  loose  material  of  much  more  recent  origin,  formed  by 
the  agency  of  ice  and  fresh  water,  so  far  as  the  evidence  goes;  and 
yet,  as  this  material  was  derived  from  the  preceding  oceanic  forma- 
tions in  great  part,  the  same  ingredients  may  and  do  occur  in  the 
water.  They  are  as  a  class  more  superficial  than  the  preceding,  and 
more  liable  to  contamination  from  surface  impurities,  and  for  a  like 
reason  their  temperature  is  often  less  constant  and  their  flow  less  reg- 
ular. While  this  is  true,  some  magnificent  springs  belong  to  this 
class.  It  will  not  be  necessary  to  enter  so  much  into  detail  here,  as 
in  many  cases  the  water-bearing  stratum  is  merely  local. 


HYDROLOGY.  145 

The  Kettle  Range  is  lined  through  its  whole  extent  with  springs. 
Its  "pots  and  kettles"  are  peculiarly  adapted  to  catch  and  tempora- 
rily hold  the  rainfall,  while  it  is  being  discharged  at  the  foot  of  the 
range,  and  at  other  convenient  points,  in  limpid  springs.  From  the 
depth  of  drift  which  the  water  penetrates,  many  of  these  become 
very  constant  in  flow  and  uniform  in  temperature.  Dousman's  mag- 
nificent trout  spring  in  the  town  of  Ottawa  probably  belongs  to  this 
class,  though  it  lies  so  near  the  great  water-bearing  horizon  between 
the  Lower  and  Upper  Silurian  formations,  that  it  may  really  originate 
there,  though  it  issues  from  the  drift.  Starin's  spring,  near  Whitewa- 
ter, the  "Big  Spring,"  near  Palmyra,  and  a  large  number  of  others  in 
the  flats  adjacent  to  the  range,  without  much  question,  have  their  res- 
ervoirs among  its  hills. 

The  numerous  lakes  along  the  range  are  largely  fed  from  similar 
sources,  which  accounts  for  the  clearness  and  purity  of  their  waters. 

Near  Lake  Michigan,  where  the  lowest  beach  deposit  rests  upon 
the  blue  bowlder  clay,  an  almost  continuous  line  of  small  rivulets  is- 
sues from  the  junction  of  the  two  formations,  the  clay  intercepting 
the  descending  water  while  the  sand  and  gravel  of  the  beach  forma- 
tion furnishes  a  ready  passage  for  it.  They  are  quite  varying  in 
chemical  character,  but  are  usually  inferior  in  purity  and  changeable 
in  temperature. 

Analagous  to  this,  there  is  another  line  along  the  lake  shore  at  the 
upper  surface  of  the  lower  red  clay,  which  is  overlaid  by  the  second 
beach  formation.  In  cause  and  character  these  are  altogether  similar 
to  the  last. 

It  would  be  fitting  in  this  connection  to  give  the  analyses  of  such 
of  the  foregoing  springs  as  have  received  quantitative  examination, 
but  a  number  of  these  have  already  been  given  by  Dr.  Lapham,  in  his 
report  on  mineral  waters,  to  which  the  reader  is  referred.  It  is 
proper  to  add  here,  however,  several  analyses  made  since  the  writing 
of  that  report. 

Wis.  Sun.— 10 


GEOLOGY  OF  EASTERN  WISCONSIN. 


SUPPLEMENTARY  TABLE  OF  ANALYSES  OF  SPRING  WATER. 


Bethesda  Springs, 
Waukesha,  by  *C. 
F.  Chandler. 

lodo-  Magnesian 
Springs,  Bcloit, 
by  C.F.  Chandlor. 

o  grH 

tT' 

White  "Rock 
Springs,  Wauke- 
sha, by  G  Bode. 

Iloreb  Mineral 
Springs,  Wauke- 
sha, by  G.  Boclo. 

Fountain  Spring, 
Waukesha,  by  J. 
V.  Z.  Blaney. 

ft  - 

tag 

«M 

£23 

0 

Chloride  of  Sodinm  

1.160 

0.&T62 

1.250 

1.170 

0.1792 

trace. 

0.470-1 

Bromide  of  Sodium     

trace. 

Iodide  of  Sodium    

0.0049 

Bicarbonate  of  Lime  

17.022 

14.5196 

16.726 

11.716 

16.7520 

13.778 

10  2704 

Bicarbonate  of  Magnesia  
Bicarbonate  of  (Soda  

12.888 
1.256 

12.280J 
0.1406 

13  142 
2.265 

5.311 
1.181 

6.  8768 

H.195 
1  021 

7.  14  JO 

Bicarbonate  of  Iron    ... 

0  042 

0  0396 

0  575 

0  048 

0  18*0 

0  1326 

Sulphate  of  Soda  ,. 

0.542 

0  524 

1.091 

1.2432 

0.360 

0  9520 

Sulphate  of  Potttssa  

0.454 

0.3123 

0  820 

Phosphate  of  Soda..  .. 

trace. 

0  0104 

0  040 

Alumina  

0.122 

0.0590 

0.720 

0.  2252 

0  097 

0.12tiS 

Silica          

0.741 

0.7581 

0  150 

1  036 

0  73ati 

0  554 

0  7SUO 

Organic  matter  

1  983 

trace. 

trace. 

0  311 

Total  per  U.  S.  gallon  of 
231  cubic  inches  

35.710 

28  5936 

38  211 

21  505 

20.0200 

25  367 

13  9126 

The  source  of  the  substances  found  in  these  springs  is  quite  clear. 
The  salts  of  lime,  magnesia,  silica,  alumina  and  iron,  are  the  rock 
substance  dissolved,  these  being  the  essential  constituents  of  the 
strata  from  which  the  waters  flow  or  through  which  they  have  per- 
colated. It  is  to  be  noted  that  the  relative  proportions  of  these  sub- 
stances in  the  analyses  bear  a  close  correspondence  to  that  which  they 
sustain  in  the  rock.  The  compounds  of  sodium  and  potassium  aro 
for  the  most  part  those  found  in  sea  waters,  whence  they  were  de- 
rived at  the  time  of  the  deposition  of  the  formations  beneath  the  Si- 
lurian ocean.  The  leaching  of  ages  has  not  sufficed  to  completely 
remove  them  from  the  interior  of  the  strata,  and  these  analyses  show 
that  they  are  still  being  dissolved  out  and  borne  back  to  the  ocean. 
The  iodine  which  distinguishes  the  Beloit  springs  is  doubtless  derived 
from  the  ancient  sea  weed  that  is  imbedded  in  abundance  in  the  rock 
from  which  its  flow  is  derived.  It  is  true,  iodine  exists  in  sea  water, 
but  in  a  much  less  proportion  than  bromine,  while  here  it  is  greater. 
It  is  further  to  be  noticed  that  the  ratio  of  iodide  of  sodium  to  chlo- 
ride of  sodium,  the  common  salt  of  the  ocean,  is  greater  than  in  sea 
water.  These  facts  warrant  the  belief  that  the  trace  of  bromine  was 
entrapped  by  the  forming  rocks  in  the  same  manner  as  the  more  com- 
mon salts,  but  that  the  iodine  arises  from  the  sea  weed  that  was 
buried  by  the  accumulating  sediments.  The  proportion  of  iodide  of 
sodium  to  chloride  of  sodium  — common  salt  —  is  greater,  with  one 
exception,  than  that  found  in  twenty-two  other  springs  containing 
iodine,  with  which  it  was  compared. 


HYDROLOGY.  147 

The  small  amount  of  organic  matter  in  these  springs  is  doubtless 
derived  from  the  surface  by  the  descending  water. 

To  enter  into  a  consideration  of  the  medicinal  character  of  those 
springs  that  have  attained  a  reputation  for  remedial  virtues,  would 
transcend  our  space,  if  not  our  province,    and  so   long  as  medical 
science  depends  rather  upon  experimental  results   than  theoretical 
considerations,  it  might  possess  little  value  if  attempted.     The  use  of 
these  waters  has  been  recommended  by  many  physicians  of   high 
standing,  and  the  results  that  have  attended  such  use  have  been  of  a 
highly  satisfactory  character.      That  there  are  differences  in  the  com- 
parative merits  of  the  several  springs  is  undoubted,  but  it  is  not  the 
prerogative  of  this  report  to  decide  between  them.     It  may  be  said  of 
them  as  a  class  that  they  are  free  from  any  excessive  amount  of  salts, 
which  are  objectionable  when  present  in  large  quantities,  though  use- 
.fnl  when  the  amount  does  not  exceed  the  demands  of  the  human 
system.     For  example,  a  certain  amount  of  lime  is  needed  by  the 
body  for  the  maintenance  of  its  bony  frame- work  and  the  perform- 
ance of  other  functions,  and  in  the  opinion  of  many  authorities  this 
may  be  advantageously  supplied  through  the  medium  of  the  water 
ingested;  but  an  excessive  amount  of   lime  salts  is  conceded  to  be 
conducive  to  certain  ailments.     If  the  amount  exceeds  that  which  can. 
be  held  in  solution  in  the  various  conditions  through  which  the  water 
passes  in  the  system,  it  is  certainly  to  be  regarded  as  excessive,  for  a 
portion  of  it  must  be  deposited.     The  quantity  of  lime  salts  of  most 
'of  the  noted  springs  elsewhere  exceeds  by  many  fold  the  average 
quantity  found  in  these.    It  is  to  be  further  noticed  that  most  of  these 
ingredients  are  invariable,  if  not  normal,  constituents  of  the  human 
body,  and  that  the  hygienic  character  of  the  water  is  beyond  question. 
It  remains  to  consider  briefly  the  geological  position  of  those  that 
have  attained  a  greater  or  less  reputation  for  medicinal  properties. 
The  Bethesda,  Hygeia,  Mineral  Rock,  White  Rock,  and  Fountain 
Springs  at  Waukesha,  flow  from  the  upper  portion  of  the  middle 
division  of  the  Niagara  limestone  which  is  capped,  in  the  vicinity, 
by  the  upper  beds,  known  as  the  Racine  limestone. 

The  Jloreb  Spring  of  this  place  issues  from  the  drift,  which  is 
here  largely  gravel  or  marly  clay  derived  from  the  above  formations. 
The  Beloit  lodo-Magnesian  Springs  flow  from  the  lower  portion  of 
the  Trenton  limestone,  a  lower  horizon  than  the  preceding  or  fol- 
lowing. 

The  Siloam  of  Milwaukee,  the  Oakton  of  Pewaukee,  the  Palmyra, 
springs,  the  Sheridan  of  Geneva,  the  Gihon  and  Barnes  of  Delavan, 
the  Nemabin  of  Oconomowoc,  Richmond's,  near  Whitewater,  and 


148  GEOLOGY  OF  EASTERN  WISCONSIN. 

the  Cedar'burg  spring,  issue  from  various  portions  of  the  drift.  It  is 
possible  that  a  concealed  connection  with  the  rock  may  exist  in  some 
of  these;  but  evidence  of  the  fact  is  wanting.  Telulah  Mineral 
Springs,  near  Appleton,  flow  from  the  drift  a  few  feet  from  the  sur- 
face of  rock  belonging  to  the  Galena  horizon,  and  from  the  fact  that 
water  of  similar  character  flows  from  a  drilling  in  the  rock  in  the  im- 
mediate vicinity,  it  is  claimed  that  the  flow  is  from  that  source. 

The  following  classified  list  of  springs,  though  far  from  being  ex- 
haustive, may  be  serviceable. 

Sulphur  Springs.  In  all  these  the  sulphur  exists  in  the  condition 
of  sulphuretted  hydrogen,  which,  being  volatile,  soon  escapes  into  the 
atmosphere,  and  so  unless  the  chemical  determination  be  made  at  the 
spring,  or  special  precautions  taken,  it  fails  to  appear  in  the  analysis. 
This  is  the  case  with  Richmond's  spring  near  Whitewater,  which  is 
very  strongly  impregnated  with  this  gas,  no  indication  of  which  ap- 
pears in  the  analysis. 

The  sulphur  is  derived  without  doubt  in  most  cases  from  the  de- 
composition of  iron  pyrites,  specimens  of  which  in  the  state  of 
decomposition  are  occasionally  to  be  found. 

PLACE.  OWNER.  SOURCE. 

Whitewater,  Sec.  1,  near  center A.  M.  Richmond Drift. 

Whitewater,  Sec.  1,  N.  W.  qr.  of  S.  E.  qr H.  J.  Starin Drift. 

La  Grange,  Sec.  9,  N.  W.  qr.  of  S.  W.  qr P.  Oleson Drift. 

La  Grange,  Sec.  36,  N.  W.  qr D.  Williams Drift. 

Appleton,  below  city J.  E.  Harriman Drift. 

Chalybeate  Springs.  These  are  characterized  by  the  presence  of 
iron  compounds,  usually  derived  from  the  decomposition  of  iron 
pyrites,  and  so  are  closely  allied  to  the  preceding. 

LOCATION  AND  CHARACTER. 

Ahnapee,  T.  25,  R.  28  E.    Sec.,  N.  W.  qr.     Temperature  45°  (August  19),  flow 

moderate  but  brisk;  little  sulphur,  much  iron,  taste  pleasant. 
Byron,  Sec.  16,  S.  E.  qr.,  large  but  not  very  strongly  impregnated. 
Empire,  Sec  18,  N.  E.  corner,  small. 

Herman,  Sec.  29,  N.  E.  qr.,  small,  but  strongly  impregnated. 
Hortonia,  on  Mr.  Briggs'  place,  Sec.  18,  two  small  springs  strongly  charged. 
Lake  Mills,  Sec.  1,  N.  hf.,  contains  also  a  little  sulphuretted  hydrogen. 
Grand  Chute,  Sec.  31,  S.  W.  qr.,  rather  small,  much  iron. 
Whitewater,  Sec.  1,  S.  E.  qr.,  limited  flow,  much  iron. 
Whitewater  Village,  small,  but  strongly  impregnated. 

Travertine  Springs.  These  contain  an  excess  of  bicarbonate  of 
lime  and  magnesia  held  in  solution  by  the  presence  of  free  carbonic 
acid  in  the  water,  which  on  escaping  into  the  atmosphere  causes  a 


HYDROLOGY.  149 

deposition  of  the  excess  of  the  lime  and  magnesia  as  travertine.  It 
frequently  coats  moss  and  other  vegetation,  which  are  then  erroneously 
said  to  be  petrified.  Where  the  base  of  the  moss  is  coated  without 
destroying  its  form,  while  the  upper  portion  is  still  green,  as  not  un- 
frequently  occurs,  the  error  is  a  very  pardonable  one.  The  deposit  is 
also  called  calcareous  tufa. 

LOCATION. 

Empire,  Sees.  6  and  7,  several. 

Hartford,  Sec.  24,  S.  W.  qr.,  several. 

Walworth,  Sees.  11,  14  and  15,  several. 

Whitewater,  Sec.  1,  near  center. 

Taycheedah,  Sec.  21,  S.  E.  qr.,  large  deposit. 

Brooklyn,  Sec.  35,  Lovers'  Glen. 

Delavan,  village,  several. 

Trout  Springs.  The  following  were  noted  as  possessing  sufficient 
volume  and  apparent  purity  to  justify  further  attention  with  a  view 
to  the  raising  of  trout.  In  the  absence  of  analyses,  their  fitness  is  not 
here  asserted  and  they  are  named  only  as  being- worthy  of  a  more 
careful  examination  by  those  who  may  be  interested.  Their  position 
in  general  is  favorable,  having  a  rapid  fall  and  being  unexposed  to 
dangerous  floods: 

LOCATION. 

Ottawa,  Sec.  14,  owned  by  W.  James. 

Ottawa,  Sec.  11,  N.  E.  qr.,  volume  limited. 

Hubbard,  Sec.  12,  N.  W.  qr.,  volume  medium. 

Hubbard,  Sec.  5,  N.  W.  qr.,  several,  medium  seize. 

Delafield,  Sec.  30,  S.  E.  qr.,  Maxwell's. 

Herman,  Sec.  5,  N.  E.  qr.,  several,  very  large. 

Herman,  Sec.  6,  N.  W.  qr. 

Theresa,  Sec.  28,  N.  E.  qr.  of  S.  E.  qr.,  large  but  perhaps  not  uniform  enough  in 

temperature. 

Ottawa,  Sec.  4,  S.  E.  qr.,  Dousman's,  already  successfully  utilized. 
Taycheedah,  Sec.  21,  S.  E.  qr.,  large. 
Taycheedah,  Sec.  16,  N.  W.  qr.  of  S.  W.  qr.,  very  large. 
Taycheedah,  Sec.  9,  S.  E.  qr.  of  S.  W.  qr.,  very  large,  rocks  colored,  but  no  iron 

taste  distinguishable. 
Ellington,  Sec.  27,  center,  large. 
Hortonia,  Sec.  28,  N.  W.  qr.,  large. 
Berlin,  Sec.  14,  Mitchell's. 
Port  Washington,  J.  Druecker's. 
Cedarburg,  now  utilized. 
Sturgeon  Bay,  opposite  village. 

Artesian  Wells.  The  term  Artesian  is  sometimes  applied  to  very 
deep  wells  without  regard  to  whether  the  water  flows  at  the  surface  or 
not,  but  it  will  here  be  confined  to  flowing  wells  without  regard  to 


150  GEOLOGT  OF  EASTERN  WISCONSIN. 

depth.  It  will  promote  clearness  of  understanding  to  call  to  mind  the 
requisite  conditions  which  will  be  found  more  amply  stated  in  Yol.  I. 
They  are  as  follows:  There  should  be  an  impervious  stratum  to  pre- 
vent the  escape  of  the  water  below;  a  previous  water-bearing  stratum 
upon  this  to  furnish  the  flow  of  water;  a  second  impervious  layer 
upon  this  to  prevent  the  escape  of  the  water  above,  it  being  under 
pressure  from  the  fountain  head.  These  must  dip,  and  there  must  be 
no  adequate  outlet  for  the  water  at  a  lower  level  than  the  well.  There 
must  also  be  a  sufficient  collecting  area  or  reservoir  in  connection 
with  the  porous  stratum  and  it  must  have  sufficient  elevation  to  act 
as  a  fountain  head.  As  these  wells  depend  for  their  essential  con- 
ditions upon  the  character  of  the  strata,  it  will  be  necessary  to  antici- 
pate some  things  subsequently  given  in  connection  with  the  formations 
involved.  To  these,  the  reader,  who  desires  a  more  perfect  under- 
standing than  can  be  obtained  from  the  necessarily  brief  sketches 
that  follow,  is  referred.  It  would  doubtless  best  subserve  the  interest 
and  convenience  of  the  general  reader,  to  classify  the  numerous  wells 
according  to  the  formation  from  which  they  derive  their  flow,  and  to 
treat  them  as  thus  grouped.  Were  this  method  pursued,  the  classes 
would  be  six  in  number,  as  follows: 

1.  Those  that  derive  their  flow  entirely  from  the  drift,  clay  layers 
forming  the  upper  and  lower  confining  strata  and  sand  or  gravel  the 
the  water-bearing  seam.     The  last  is  usually  a  beach  deposit  and  at 
least  one  of  the  others  a  lacustrine  clay.     This  group  includes  the 
fountains  of  Taycheedah,  Calumet,  Poysippi,  Rushford,  Auroraville, 

Whitewater,  Byron,  and  a  part  of  those  of  Fond  du  Lac,  Oakfield, 
and  Oshkosh,  with  some  in  the  vicinity  of  Lake  Michigan. 

2.  Those  that  derive   their  flow  from  the  junction  of  the  drift 
with  the  indurated  rocks  below.     In  these  the  drift  clays  resting  on 
the  rock  constitute  the  upper  confining  stratum  and  the  subjacent  for- 
mations, the  lower,  while  a  layer  of  sand  or  gravel  or  the  open  nature 
of  the  rock  surface  affords  passage  for  the  water.     This  class  includes 
most  of  the  fountains  at  Fond  du  Lac,  Oshkosh,  Oakfield,  and  Green 
Bay. 

j.  Those  that  originate  in  the  Niagara  limestone.  This  body  of 
limestone  furnishes  in  itself,  locally,  the  necessary  pervious  and  iia- 
pervious  strata.  The  Manitowoc  wells  belong  here. 

^.  Those  that  arise  from  the  Galena  and  Trenton  limestones. 
These  formations,  like  the  Niagara,  aided  by  the  overlying  drift,  pre- 
sent all  the  needed  conditions.  There  are  embraced  here,  most  of  the 
Watertown  fountains  and  a  portion  of  those  at  Oshkosh  and  Fond 
du  Lac. 


<  .\/  1 1 

VM' 


<>/• 


PLATE.V 


PROFILES  ILLUSTRATINCr  ARTESIAN  WEI^LS 

~by  T.  C.  Chamlierlin  . 

Stctiott  frcni 
TAYCHEDAH  TO    RIPON 

netL  .  Vert.Scalr  2OOf>  i  //nrft-  . 


Profile  from 
LAKK   WINNEBAGO  TO    SEC.  3O    BYRON 


Profile  frorn. 

SEC.  1O  BYRON  TO    SEC.  2*  WAUPITN 
Har.ScattSMOra-Jlnrh.  Vrrt.Scalc  iOJn^ 


Profile  from, 

THE  NORTHERN  HOSPITAL  FOR  THE  INSANE  TO  THE  TOWN  OF  CALEDONIA       ^  g.     ^ 
Hor. Stale 2MSfs-1  Inch  .  T/rrt..Srale  2000ft-  1  fnrh  .  5  *       * 


LAKE  POYGAWIVESTWARB 


Lah-r I'pygan 


Profile  from. 

TVBITEWATER  TO  HEART  PRAIRIE, 
Her.  Scott  SMila=1lntti.  Vert.Scale  SOOfl  -.  /  Inrh 

KettJeKangr 


^  Kettles  "       Heart  f^afn'r 


HYRDROLOGY.  151 

5.  Those  from  the  St.  Peters  sandstone.     This  is  by  far  the  most 
widely  available,  and,  except  locally,  the  most  important  source  of  Ar- 
tesian wells  in  eastern  Wisconsin.     The  lower  layers  of  the  Trenton 
limestone,  resting  upon  it,  form  an  efficient  confining  sheet  above, 
and  the  formations  below  are  saturated  by  water  having  a  higher 
source  than  that  of  the  St.  Peters  sandstone,  so  that  there  can  be  no 
loss,  but  may  be  gain  from  beneath.     Aside  from  the  porous  charac- 
ter of  the  sandstone,  it  is  much  fissured  in  vertical,  oblique  and  ir- 
regular directions,  enabling  the  water  to  readily  traverse  it.     From 
this  horizon  arise  the  deeper  seated  fountains  at  Watertown,  Wild's 
well  and  several  more  recently  sunk  at  Fond  du  Lac,  the  "oil  well " 
at  Palmyra,  the  exceptionally  saline  well  at  Sheboygan,  and  those  at 
Milwaukee,  Racine  and  Western  Union  Junction. 

6.  Those  from  the  primordial  zone.     The  well  at  the  Northern, 
Hospital  for  the  Insane,  at  Oshkosh,  represents  this  class.     The  pub- 
lic well  on  Algoma  street,  Oshkosh,  the  water  of  which,  though  it  does 
not  flow  at  the  surface,  rises  within  a"  few  inches  of  it,  may  be  also 
classed  here.   '  So  also  the  well  on  the  Fair  Grounds  at  Janesville, 
which  flows  through  the  aid  of  hydraulic  appliances.     A  portion  of  the 
flow  of  the  Racine  well  is  from  this  horizon. 

These  six  classes,  it  may  again  be  remarked,  furnish  the  most  sys- 
tematic grouping  for  study  and  description,  but  it  will  doubtless  be 
most  convenient  and  interesting  to  the  people  of  the  state  for  whose 
benefit  the  survey  was  instituted,  to  describe  these  wells  by  the  local- 
ities in  which  we  find  them  situated. 

In  number  and  variety  of  source,  the  flowing  wells  of  Fond  duLac 
stand  preeminent.  They  represent  four  of  the  six  systems  above 
mentioned.  The  accompanying  profiles  represent  much  more  clearly 
and  satisfactorily  the  conditions  under  which  these  fountains  are  se- 
cured than  an  elaborate  description,  and  will  only  need  to  be  sup- 
plemented by  some  additional  and  explanatory  statements.  And  I 
desire  here  to  express  my  special  indebtedness  for  many  facts,  other- 
wise beyond  my  reach,  to  Mr.  C.  O'Connor,  who  has  sunk  many  of 
these  wells.  From  his  statements  it  appears  that  there  are  three 
classes  of  comparatively  shallow  wells  that  derive  their  flow  from 
within  twenty  feet  of  the  surface  of  the  rock,  either  above  or  below 
it,  it  being  from  two  to  nearly  one  hundred  feet  beneath  the  soil.  In 
the  first,  flowing  water  is  found  in  the  blue  clay  which  underlies  the 
superficial  red  clay.  The  water  is  usually  reached  in  a  stratum  of 
quicksand,  from  six  inches  to  six  feet  in  thickness.  In  the  second, 
the  flow  is  obtained  between  what  is  locally  known  as  the  "concrete" 
and  the  rock.  This  concrete,  which  varies  from  two  to  twenty  feet 


152  GEOLOGY  OF  EASTERN  WISCONSIN. 

in  thickness,  is  the  lowest  member  of  the  drift  at  this  point,  and 
seems  to  consist  of  partially  cemented  sand  and  gravel.  The  first  flow 
of  water  is  usually  accompanied  by  a  green  or  brown  sand.  The 
flow  of  the  third  class  originates  in  the  rock,  within  from  six  to 
twenty  feet  of  its  surface,  and  is  unaccompanied,  in  general,  by  sand 
of  any  kind.  The  vast  majority  of  the  wells  of  the  city  belong  to  one 
of  these  three  classes.  The  generous  well  of  Mr.  George  Hunter, 
known  as  "Hunter's  Magnetic  Saline  Fountain,"  derives  its  flow 
from  the  deeper  limestone  strata,  as  is  shown  from  the  following  sec- 
tion furnished  through  the  kindness  of  the  proprietor: 

Feet. 

Red  clay 26 

Blue  clay,  bowlders  and  concrete 30 

First  water  course  at 56 

Brown  limestone 14 

Second  watercourse  at 70 

Brown  limestone 40 

Third  watercourse  at 110 

White  limestone 30 

Fourth  water  course  at 140 

Crystalline  cherty  limestone 20 

Cherty  limestone 27 

Fifth  water  course  at 187 

Total  depth  187 

The  following  is  an  analysis  of  the  rock  taken  from  this  well,  made 
by  Rev.  A.  C.  Barry: 

Lime 28.90 

Magnesia 20.76 

Protoxide  of  iron 2. 19 

Soda 20 

Chlorine trace . 

Sulphuric  acid 10 

Carbonic  acid 45 . 51 

97.66 


From  which  it  appears  that  this  rock,  in  common  with  nearly  all 
so-called  limestone  of  eastern  Wisconsin,  is  really  a  doloniite.  The 
following  is  the  analysis  of  the  water  of  this  well,  published  by  the 
proprietor.  As  the  form  is  somewhat  unusual,  the  letter  communi- 
cating it  is  published: 

KEOKUK  MEDICAL  COLLEGE,  February  9,  1874. 
GEOBGK  HUNTER,  ESQ.  : 

Dear  Sir:  —  I  have,  to-day,  completed  the  quantitative  analysis  of  your  mineral  water, 
and  with  the  following  results.  Out  of  one  gallon  of  water  I  obtained  19  grains  as 
residuum. 


HYDROLOGY.  153 

The  analysis  is  an  approximate,  leaving  off  decimals  in  calculating  the  proportions. 
In  100  parts,  the  following  are  the  proportions  of  each  ingredient: 

1.  Carbonate  of  lime 5 

2.  Carbonate  of  potash 4 

3.  Carbonate  of  magnesia 6 

4.  Carbonate  of  soda 4 

5.  Sulphate  of  lime 12 

6.  Sulphate  of  potash , 10 

7.  Sulphate  of  magnesia 17 

8.  Sulphate  of  soda 13 

9.  Chloride  of  sodium 14 

10.  Chloride  of  potassium 3 

11.  Silica 5 

93 

12.  Traces  of  iron — 

14.  Traces  of  bromine — 

14.  Free  carbonic  acid — 

Wa^te 7 

100 

To  my  surprise,  I  found  a  trace  of  bromine  in  it.  1  did  not  estimate  the  free  carbonic 
acid.  Very  respectfully  yours,  E.  J.  GILLETT. 

The  water  has  been  extensively  used  for  its  remedial  qualities. 
The  magnificent  fountain  on  First  street,  belonging  to  Messrs.  B. 
"Wild  &  Co.,  represents  a  yet  more  deep  seated  system.  This  well  is 
326  feet  deep,  and  passes  entirely  through  the  Galena  and  Trenton 
limestones,  reaching  the  St.  Peters  sandstone  below,  whence  it  derives 
a  flow  of  forty-eight  gallons  per  minute.  The  stream  has  been  carried 
by  pipes  53  feet  above  the  surface.  It  flows  with  such  force  that, 
with  hose  and  quarter-inch  nozzle  attached,  it  projects  a  stream  from 
30  to  35  feet  high,  and  48  feet  horizontally.  An  analysis  of  the  water 
of  this  well  will  be  found  in  the  report  of  Dr.  Lapham,  ante,  p.  31,  of 
this  volume. 

The  following  is  the  section  of  the  well  on  the  high  school  grounds, 
kindly  furnished  by  Senator  "W.  H.  Hiner: 

Feet. 

Drift,  red  and  blue  clay 95 

Magnesian  limestone  (Trenton  and  Galena) 195 

St.  Peters  sandstone 135 

Total 425 

In  searching  for  the  fountain  head  of  the  first  class,  or  those  which 
belong  entirely  to  the  drift,  we  find  possible  sources  on  almost  every 
side,  to  the  east,  south,  west  and  northwest.  To  the  east  and  south 


154  GEOLOGY  OF  EASTERN  WISCONSIN. 

there  lies  a  ledge  of  Niagara  limestone,  underlaid  by  impervious  shale 
from  the  surface  of  which  issue  frequent  springs.  The  clay  deposits 
of  the  basin,  in  which  the  city  lies,  abut  against  and  overlap  this  shale. 
The  junction  is  in  all  probability  permeable  to  water,  which  would 
thus  reach  the  porous  strata  of  sand  and  gravel  that  are  found  within 
the  blue  clay.  That  this  is  the  true  explanation  of  the  Artesian  wells 
of  Taycheedah  and  Byron  is  more  than  probable.  To  the  west,  the  blue 
clay  rises  to  the  surface  and  lies  upon,  or  graduates  into,  the  more 
gravelly  drift  hills  of  that  region,  and  may  not  improbably  derive  its 
water  supply  from  thence. 

The  fountain  heads  of  the  second  and  third  classes,  viz.:  those  that 
rise  from  the  concrete  and  from  the  limestone,  are  doubtless  the  same, 
or  at  least  their  fountain  heads  are  associated,  except  perhaps  those  of 
the  deep  wells,  whose  reservoir  is  more  distant;  in  all  cases  it  is 
probably  to  the  westward.  Lamartine  and  adjoining  townships  furn- 
ish favorable  conditions.  The  surface  of  the  rock,  as  well  as  its  lay- 
ers, rise  in  that  direction.  The  slight  local  exception  to  this  in  the 
western  portion  of  the  city  is  not  sufficient  to  afiect  the  general  prob- 
lem. The  rock  appears  at  the  surface  to  the  southwest,  along  Seven 
Mile  creek,  at  an  elevation  of  122  feet  above  Lake  Winnebago.  The 
general  surface  of  the  town  of  Lamartine  is  about  150  feet  above  Lake 
"Winnebago,  if  a  single  series  of  aneroid  measurements  is  to  be  trusted, 
and  consists  of  low  hills  and  ridges  interspersed  with  marshes.  The 
surface  drainage  is  very  imperfect.  The  hills  and  ridges  are  com- 
posed of  the  varying  mixed  material  of  the  unassorted  drift,  and  are 
more  or  less  permeable  to  water. 

Phenomena  connected  with  the  boring  of  wells  in  this  region  show 
that  certain  of  the  layers  of  the  underlying  magnesian  limestone  are 
practically  impervious  to  water,  while  others  are  not.  These  with  the 
clay  above  furnish  the  necessary  pervious  and  impervious  strata,  and 
complete  the  requisite  conditions. 

The  fountain  head  of  Mr.  "Wild's  well  is  to  be  found  along  the  line 
of  outcrop  of  the  St.  Peters  sandstone  within  which  its  reservoir  un- 
doubtedly lies.  Near  Bipon,  the  St.  Peters  sandstone  outcrops  at  an 
elevation  of  about  325  feet  above  Lake  Michigan,  or  about  150  feet 
above  the  surface  of  the  well,  thus  giving  an  abundant  elevation. 

The  flowing  wells  of  Taycheedah  are  from  60  to  70  feet  deep,  but 
do  not  reach  the  rock.  It  seems  most  probable  that  they  derive  their 
flow  from  veins  having  their  origin  at  the  surface  of  the  shale  beneath 
the  ledge,  as  already  explained,  and  as  shown  in  the  sections.  The 
water  in  some  of  the  wells  is  highly  impregnated  with  sulphuretted 
hydrogen. 


HYDROLOGY.  155 

In  the  town  of  Byron,  adjoining  Fond  du  Lac  on  the  south,  on  the 
farms  of  Mr.  Henry  Bush,  Mr.  D.  D.  Jones,  and  Mr.  Searles,  there 
are  several  wells  having  a  rather  scanty  and  variable  flow.  They  are 
not,  however,  immediately  affected  by  rains.  The  wells  belonging  to 
Mr.  Jones  are  TO  feet  in  depth.  The  vein  was  found  in  a  bed  of 
quicksand  at  least  10  feet  thick.  Rock  was  struck  at  Mr.  Searles'  at 
a  depth  of  170  feet  —  but  did  not  yield  a  flow.  The  fountain  head  of 
these  is  probably  in  the  bluffs  to  the  south,  as  indicated  in  the  profile. 

The  Artesian  wells  of  the  town  of  Oakfield  are  located  in  sections 
9, 15, 16  and  IT,  and  occupy  an  extensive  depression  stretching  north- 
eastward to  Fond  du  Lac.  Mr.  II.  D.  Hitt  has  three  wells  from  68  to 
T4  feet  deep.  He  gives  the  following  as  a  typical  section: 

1.  Surface  soil. 

2.  Marl. 

3.  Blue  clay. 

4.  Small  vein  of  sand. 

5.  Alternating  blue  clay,  sand  and  gravel. 

6.  Rock  at  from  48  to  54  feet  from  the  surface. 

Water  flowed  in  a  small  stream  before  the  rock  was  struck.  On 
the  same  authority  I  learn  that  Mr.  "Whittaker  secured  a  fine  stream 
in  a  vein  of  sand  beneath  blue  clay,  at  from  20  to  22  feet  from  the 
surface.  Mr.  S.  Scovil,  residing  on  section  IT,  has  two  flowing  wells, 
one  48  feet  and  the  other  T5  feet  deep.  The  former,  as  I  was  inform- 
by  the  proprietor,  is  3T  feet  in  blue  clay  and  12  feet  in  limestone.  It 
is  situated  near  the  western  extremity  of  the  depression  before  men- 
tioned, where  the  surface  gradually  rises  toward  the  drift  hills  that 
form  the  "divide"  between  the  Mississippi  and  St.  Lawrence  basins. 
The  latter  lies  somewhat  farther  eastward,  and  penetrates  50  feet  o£ 
pure  clay  without  seams  of  sand  or  gravel,  and  extends  25  feet  into 
the  limestone  beneath.  This  well  has  a  brisk  steady  flow  about  one 
inch  in  cross  section,  and  is  not  noticeably  affected  by  rains.  The 
former  one,  when  visited,  had  but  a  slight  stream  which  broke  into 
drops  in  falling  six  inches,  and  was  said  to  be  much  affected  by  rains, 
the  change  being  noticeable  within  24  hours.  The  wells  of  Mr.  Hatch 
and  Mr.  "Wells  are  similarly  affected.  These  are  said  not  to  penetrate 
the  rock.  We  gather  from  these  facts  that  there  are  two  systems 
here,  the  more  superficial,  whose  veins  lie  near  the  junction  of  tho 
drift  and  limestone,  being  sometimes  above  and  sometimes  below,  and 
whose  reservoir  is  in  the  vicinity  and  is  superficial;  and  the  deeper 
one,  whose  fountain  head  is  more  distant.  The  reservoirs  in  both 
cases  are  probably  to  the  westward  or  northwestward. 


156  GEOLOGY  OF  EASTERN  WISCONSIN. 

The  shallower  system  of  Artesian  wells  at  Oshkosh  is  quite  similar 
to  that  of  Fond  du  Lac,  already  described.  They  vary  in  depth  from 
15  to  100  feet,  and  derive  their  flow  variously  from  within  the  drift, 
at  the  surface  of  the  rock,  and  at  varying  depths  within  it.  The 
source  of  their  supply  is  undoubtedly  to  the  westward  and  less  than 
ten  miles  distant. 

The  deeper  wells  possess  unusual  interest  from  the  facts  they  de- 
velop relating  to  the  strata  beneath.  Unfortunately  no  complete 
record  of  the  formations  passed  through  in  sinking  the  well  at  the 
Northern  Hospital  for  the  Insane  seems  to  have  been  made,  and  noth- 
ing is  now  available  but  the  very  general  statements  of  the  person 
who  drilled  the  lower  portion,  and  an  inspection  of  the  mingled  drill- 
ings at  the  well.  These  showed  that  variously  colored  sandstone 
strata  had  been  penetrated  to  a  considerable  depth,  and  that  a  reddish 
granitic  rock  had  been  entered. 

The  following  items  were  furnished  by  Mr.  J.  II.  Johnson,  who 
drilled  the  lower  portion: 

Struck  limestone  at 60  feet. 

sandstone  at 300 

water  at 800 

red  sandstone  at 540 

white  sandstone  at 585 

granite  at 714 

white  granite  at 935 

Bottom..                                                                                  .  961 


Mr.  Johnson  expressly  stated  that  below  300  feet  it  was  all  sand- 
stone till  the  granite  was  reached. 

In  regular  order  we  should  expect  in  descending,  Trenton  lime- 
stone, the  St.  Peters  sandstone,  the  Lower  Magnesian  limestone,  and 
the  Potsdam  sandstone,  including  a  calcareous  stratum,  and  the  gran- 
itic rocks  at  the  bottom  as  found.  The  question  is  naturally  sug- 
gested, Is  the  St.  Peters  sandstone  wanting,  bringing  the  Trenton 
and  Lower  Magnesian  limestones  together;  or  is  the  Lower  Magne- 
sian limestone  wanting  as  such,  bringing  the  St.  Peters  and  Pots- 
dam sandstones  together? 

Much  light  is  thrown  on  this  interesting  question  by  the  very  excel- 
lent record  and  the  drillings  of  a  public  well,  subsequently  sunk  within 
the  city  of  Oshkosh,  preserved  by  Mr.  K.  M.  Hutchinson,  and  sub- 
mitted to  me  by  the  kindness  of  Dr.  Lapham. 

The  record  is  incorporated  in  my  notes,  on  an  examination  of  the 
drillings,  which  are  as  follows: 


HYDROLOGY.  157 

1.  Drift  92  feet. 

2.  From  92  to  300  feet,  a  hard,  bluish-grey,  close-textured,  semi- crystalline  magnesian 
limestone.     A  few  scales  of  sesqui  oxide  of  iron  present. 

3.  At  300  feet,  reddish,  calcareous  clay,  containing  angular  fragments  of  limestone 
and  sesqui  oxide  of  iron. 

4.  At  308  feet,  chiefly  red  silicious  sand  of  varying  coarseness,  mixed  with  fragments 
of  dark  shale. 

5.  At  400  feet,  light  orange,  silicious  sand,  the  constituent  grains  of  which  are  irregu- 
lar in  form  and  surface.     White  clay-hke  fragments,  appearing  like  kaolin,  and  insolu- 
ble in  hydrochloric  acid,  probably  chippings  of  soft  chert,  also  present. 

6.  At  416  feet,  dirty  red  sand,  mingled  with  fragments  of  magnesian  limestone,  and 
also  lumps  of  sand  and  limestone  cemented  with  a  reddish  or  whitish  calcareous  clay. 

7.  At  425  feet,  white  and  orange,  rather  coarse,  silicious  sand,  and  a  little  of  the  kaolin- 
like  material,  almost  all  the  fragments  of  which  are  marked  upon  one  side  by  metallic 
iron,  evidently  from  the  drill,  showing  that  they  were  clipped  with  difficulty  from  a 
larger  mass. 

8.  At  435  feet,  yellowish-orange,  silicious  sand;  the  grains  of  medium  size,  and  numer- 
ously marked  with  adherent  specks  of  oxide  of  iron.     Many  fragments  of  chert  drillings, 
marked  with  metallic  iron,  also  present. 

9.  At  500  feet,  very  fine  grained  silicious  sand;  a  few  minute  lumps  consisting  of  grains 
of  sand  cemented  by  finer  material;   no  effervescence  in  heated  or  cold  hydrochloric 
acid;  color,  yellowish  white;  some  chert  drillings  present. 

10.  At  557  feet,  drillings  light  pinkish  grey,  appearing  like  crystalline  powder.     Ex- 
amined under  microscope,  found  to  be  composed  of  grains  of  limpid  quartz  and  particles 
of  chert  associated  with  the  more  finely  powdered  material  that  gives  rise  to  the  color. 
No  effervescence  when  tested  with  cold  or  hot  hydrochloric  acid. 

11.  From  580  feet  to  618  feet,  the  drillings  are  similar  to  the  above,  but  the  quartz 
grains  are  larger,  more  numerous  and  conspicuous,  and  the  finer  material  is  white. 
A  very  small  amount  of  oxide  of  iron  is  present.    No  action  when  treated  with  acid. 

12.  From  685  feet  to  695  feet,  orthoclase  feldspar  predominates,  attended  by  consid- 
erable quartz  and  a  less  quantity  of  a  dark  mineral,  probably  hornblende. 

Classified,  the  two  sections  become: 

At  Hospital.  On  Algoma  St. 

Drift 60  feet.  92  feet. 

Limestone 240    "  208    " 

Sandstone 414    "  380    " 

Graniterock 248     "  15    " 


Total 961  feet.  695  feet. 


The  correspondence  between  the  two  is  quite  marked.  In  the 
southwestern  portion  of  the  city  the  rock  of  the  region  is  exposed  in 
quarries  at  an  elevation  very  nearly  the  same  as  the  surface  at  these 
wells.  This  rock  is  clearly  shown  by  its  fossils  to  belong  to  the  Ga- 
lena limestone,  in  the  modified  character  which  that  formation  bears 
in  this  region.  It  is  seemingly  the  lower  portion  of  the  formation, 
and  there  is  good  reason  for  believing  it  to  be  entirely  wanting  at  the 
locality  of  the  wells  where  the  drift  is  deep.  The  lower  strata  of  the 
Trenton  limestone  are  found  at  the  surface  at  a  distance  of  less  than 


158  GEOLOGY  OF  EASTERN  WISCONSIN. 

six  miles  to  the  west.  Now  between  Ripon  and  Fond  du  Lac,  along 
a  parallel  and  not  distant  line,  the  dip  of  the  lower  face  of  the  Tren- 
ton limestone  is  accurately  ascertained  to  be  23  feet  per  mile  to  the 
eastward.  Calculating  upon  the  basis  of  this  dip,  and  making  allow- 
ance for  the  drift,  there  should  be  less  than  fifty  feet  of  the  Trenton 
limestone  at  the  location  of  the  well  on  Algoma  street. 

This  result  is  confirmed  by  calculations  based  on  different  data,  and 
by  a  general  inspection  of  the  problem.  Assuming  this  to  be  correct, 
the  thickness  of  limestone  below  is  sufficient  to  occupy  the  whole 
horizon  of  the  St.  Peters  sandstone  and  Lower  Magnesian  limestone; 
or  in  other  words,  the  208  feet  of  limestone  in  the  one  case,  and  the 
240  feet  in  the  other,  just  about  fill  up  the  space  that  we  should  ex- 
pect would  be  occupied  by  the  Trenton,  St.  Peters,  and  Lower  Mag- 
nesian formations.  What  then  has  become  of  the  St.  Peters  sandstone? 
One  of  the  more  recent  discoveries  of  the  survey  makes  this  perfectly 
clear.  The  upper  surface  of  the  Lower  Magnesian  limestone  in  this 
region  is  very  undulating;  we  might  say,  billowy.  The  St.  Peters 
sandstone  lies  in  the  troughs  between  these  billows,  and  usually  cov- 
ers their  crest,  but  sometimes  the  Trenton  rests  directly  upon  the 
elevated  portions  of  the  lower  limestone,  and  the  St.  Peters  sandstone 
is  entirely  wanting.  This  has  actually  been  observed  in  some  cases, 
and  drilling  at  other  points  has  left  no  doubt  that  this  is  not  an  un- 
common fact.  If  we  suppose  then  that  the  Trenton  limestone  here 
rests  directly  on  the  Lower  Magnesian  as  it  does  near  Ripon,  the 
whole  of  the  difficulty  disappears.  See  Plate  YI. 

The  calcareous  material  found  in  the  sandstone  below,  doubtless 
represents  the  Mendota  limestone,  and  must  be  regarded  as  confirm- 
ing the  above  conclusions. 

The  well  at  the  Hospital  discharges  about  22,000  gallons  per  day. 
This,  accepting  the  foregoing  views,  is  derived  from  the  Potsdam 
sandstone,  below  the  calcareous  Mendota  stratum.  Its  collecting  area 
is  probably  twenty-five  miles  to  the  northwestward,  and  has  but  a 
slight  elevation. 

At  the  mill  of  W.  N.  Davis,  on  the  shore  of  lake  Winnebago,  in 
Calumet,  are  two  fine  wells,  giving  a  copious  flow  of  clear,  cold, 
sparkling  wrater,  impregnated  with  considerable  iron  and  some  sul- 
phuretted hydrogen.  The  proprietor  gave  the  depth  as  about  90  feet, 
but  was  not  certainly  informed  whether  rock  was  reached  or  not,  as 
the  well  was  not  sunk  by  him.  These  are  probably  to  be  classed  with 
fhe  Taycheedah  wells,  having  their  source  to  the  east,  though  it  is  not 
impossible  that  they  belong  to  the  Oshkosh  system,  as  the  fountains 
surrounding  the  lake  indicate  that  its  bed  is  impervious. 


HYDROLOGY.  159 

The  Lake  Winnebago  System.  All  the  drift  wells  of  Oshkosh,  Fond 
du  Lac,  Taycheedah,  Calumet,  and  their  vicinity,  may  be  considered  as 
constituting  one  group,  owing  their  origin  to  the  basin-shaped  de- 
pression occupied  by  the  lake,  the  superficial  layer  of  which  is  imper- 
vious and  prevents  the  wrater  from  escaping  into  the  lake  until  pierced. 

The  wells  at  Green  Bay  and  other  points  in  the  valley  of  the  lower 
Fox  river  derive  their  flow  from,  at,  or  near  the  surface  of  the  rock, 
and  may  be  classed  with  the  above  system. 

The  Poygan  Lake  System.  The  numerous  wells  in  Rushford, 
Aurora,  Poysippi  and  vicinity,  are  located  in  part  in  the  valley  of  the 
Fox  river,  but  they  all  belong  to  a  common  depression  filled  by  a  con- 
tinuous lacustrine  clay  deposit,  and  are  essentially  alike  in  nature  and 
origin.  They  all  belong  to  the  drift,  and  owe  their  existence  to  the 
alternate  porous  and  impervious  character  of  the  red  clay  and  associ- 
ated beach  deposits.  The  surface  of  the  area  is  level  and  considerably 
below  that  of  the  surrounding  country.  The  flow  is  obtained  at  vari- 
ous depths,  but  not  without  some  degree  of  uniformity,  giving  rise  to 
the  popular  terms  "  forty  foot  vein  "  and  "  eighty  foot  vein."  The 
wells  rarely  exceed  100  feet  in  depth. 

The  material  penetrated  is  usually  red  clay,  with  occasional  seams 
of  sand  and  gravel,  the  whole  attaining  a  thickness  of  from  80  to  100 
feet.  There  seems  good  reason  for  considering  the  "  forty  foot  vein  " 
as  being  derived  from  the  beach  deposit  between  the  upper  and  lower 
red  clays  hereafter  to  be  described,  and  the  "  eighty  foot  vein "  as 
corresponding  to  the  beach  formation  between  the  lower  red  clay  and 
the  blue  bowlder  clay.  These  beach  deposits  are  preeminently  porous 
and  water-bearing  elsewhere  in  the  state,  and  from  the  nature  of  the 
led  clay  it  would  be  difficult  to  account  for  two  veins  so  persistent  as 
these  seem  to  be,  on  any  other  supposition.  These  wells  frequently 
interfere  with  those  near  them  so  that  it  is  necessary  to  adjust  the 
penstocks  to  the  same  level.  This  shows  that  they  are  derived  from 
a  common  stratum,  and  lends  support  to  the  view  given  above.  The 
flow  is  usually  brisk  and  abundant,  and  in  some  cases  is  very  copious. 
The  water  is  mostly  excellent  and  generally  rather  soft.  Occasionally 
it  is  impregnated  with  iron  and  sulphur. 

The  source  of  the  flow  of  these  wells  is  quite  obvious.  The  clay 
strata  terminate  on  the  margin  of  the  basin  adjacent  to  and  in  asso- 
ciation with  sandy  drift  hills  of  highly  absorbent  character.  Around 
the  rim  of  the  basin  thus  constituted  the  water  finds  access  to  the 
porous  layers  and  through  them  supplies  the  fountains.  The  num- 
ber of  these  wells  is  large  and  constantly  increasing,  as  the  clay  may  be 
bored  with  the  greatest  facility  and  at  trifling  cost. 


160  GEOLOGY  OF  EASTERN  WISCONSIN. 

The  Artesian  wells  of  Watertown  belong  to  two  classes,  the  one, 
including  the  greater  number,  arising  from  the  Trenton  limestone, 
the  other  embracing  the  deeper  wells  from  the  St.  Peters  sandstone. 
The  first  class  vary  in  depth  from  18  feet  to  100  feet;  the  second 
from  the  latter  depth  to  215  feet. 

One  of  the  most  interesting  of  the  latter  class  is  located  near  the 
shops  of  the  Milwaukee  &  St.  Paul  Bail  way  Company,  to  whom  it 
belongs.  The  following  record  was  furnished  Dr.  Lapham  through 
the  kindness  of  Mr.  G.  W.  Waring,  who  superintended  the  work  of 
sinking  it: 

Depth  of  soil 50  feet. 

Depth  of  limestone 57     " 

Depth  of  sandstone 108    " 

Total..  .  215    " 


"Water  began  to  flow  when  a  depth  of  107  feet  was  reached,  and 
could  be  raised  10  feet  above  the  surface. 

The  two  following  brief  records  will  sufficiently  illustrate  this  class. 
They  were  furnished  through  the  courtesy  of  Mr.  S.  S.  Woodward, 
who  has  taken  a  deep  interest  in  the  subject: 

Drift 10  feet.  15  feet. 

Limestone ." 93    "  103    " 

Sandstone .• 23    " 


Total 103    "  141 


If  we  assume  that  the  flow  of  the  former  was  from  the  surface  of 
the  St.  Peters  sandstone,  the  upper  face  of  the  sandstone  will  be  107 
feet,  103  feet,  and  118  feet,  respectively,  below  the  surface,  at  the 
three  wells,  facts  which  may  be  of  service  in  sinking  others. 

The  first  one,  that  of  the  Eailway  Co.,  is  243  feet  above  Lake  Mich- 
igan, and  hence  its  bottom  is  28  feet  above  the  lake  level. 

The  source  of  supply  for  both  classes  seems  to  lie  to  the  west  of 
north,  where,  both  near  and  distant,  occur  many  depressions  entrapped 
between  limestone  and  drift  ridges,  giving  abundant  superficial  reser- 
voirs, while  in  this  direction  also  may  be  found  the  outcropping  edge 
of  the  sandstone.  This  sandstone  likewise  comes  to  the  surface  to  the 
west  of  Watertown,  but  the  low  elevation  in  that  region  seems  to  in- 
dicate that  the  flow  is  not  from  that  quarter.  The  western  edge  of 
the  sandstone,  where  it  comes  to  the  surface,  follows  the  east  bank  of 
the  Crawfish  river,  from  Lowell  to  Aztalan,  and  at  no  point  between 
those  places  has  it  an  elevation  much  greater  than  the  railroad  junc- 
tion at  Watertown.  It  is  not  to  be  expected  then  that  fountains  can 
be  obtained  from  the  St.  Peters  sandstone,  which  will  flow  at  a  much 


PLAT.  V3 


HYDROLOGY.  161 

greater  elevation  than  that  already  attained,  viz. :  253  feet  above  Lake 
Michigan.  By  penetrating  the  Potsdam  sandstone  there  is  a  reason- 
able probability  that  a  flow  competent  to  rise  to  a  higher  elevation 
could  be  obtained. 

The  following  is  an  analysis  of  the  water  of  Mr.  Buckhert's  fountain, 

by  Dr.  L.  Brandecke: 

Grains  in  1  gal, 

Bicarbonate  of  soda 1.898 

Bicarbonate  of  magnesia 5.818 

Bicarbonate  of  lime , 12.094 

Bicarbonate  of  iron 0.100 

Sulphate  of  potassa 0.054 

Silica 0.305 

Organic  matter 0.346 

Total..  .   20.615 


While  the  above  mentioned  facts  are  still  in  mind,  it  will  be  con- 
venient to  speak  of  the  Palmyra  "  oil  well."  A  failure  as  a  source  of 
oil,  it  yet  has  proved  of  some  value  in  demonstrating  the  possibility  of 
Artesian  wells  in  that  and  similar  situations.  The  following  is  the  rec- 
ord kindly  furnished  me  by  Dr.  Lapham : 

Palmyra  Artesian  Well  (1865).  Begun  about  250  feet  above  Lake 
Michigan  (828  feet  above  the  sea). 

46  feet.  Drift  —  struck  limestone. 
176  "      Limestone;  supposed  to  be  "  Blue  Limestone." 
229   "      Water. 
235  "      Slate  and  sand. 
255  "      "Good  show  of  oil."  (!) 
257  "      "Big  show  of  oil."  (!!)  Struck  sand  rock. 
263  "      Great  flow  of  water. 
283  "      Metal  2  inches.    (Iron  ore  ?). 

350  "      Supposed  Lower  Magnesian  limestone;  Calciferous  sand  rock. 
412  "      White  sandstone. 
421   "      Gray  sandstone. 
455  "      Red  sandstone. 
461   "      Black  sandstone. 

Hard  sandstone,  3  feet. 
1      Gray  sandstone. 

Soft  sandstone. 

Hard  sandstone. 

Soft  sandstone. 
;  Red  sandstone. 
;  Gray  sandstone. 

Red  sandstone. 

Drab  or  cream  colored  sandstone. 

Soapstone  or  shale. 

Gray  sandstone  to  bottom  of  well. 

Bottom  of  well,  being  500  feet  below  Lake  Michigan;  78  above  the  sea. 
Wis.  SUE.— 11 


162  GEOLOGY  OF  EASTERN  WISCONSIN. 

These  may  be  distributed  as  follows: 
46  feet.  Drift. 


130 
81 
93 
62 


Galena  limestone. 
Trenton  limestone. 
St.  Peters  sandstone. 
Lower  Magnesian  limestone. 
Potsdam  sandstone. 


The  flow  is  derived  from  the  St.  Peters  sandstone.  It  cannot  have 
its  source  in  that  formation  directly  to  the  west,  since  the  outcrop  is. 
lower  than  the  surface  of  the  well.  The  fountain  head  is  probably 
in  the  same  region  as  that  of  the  Watertown  wells  of  its  class.  I  was 
told  that  originally  the  stream  was  very  large,  and  could  be  raised  30 
feet  above  the  surface,  but  at  the  time  of  my  visit  it  was  meager,  and 
would  rise  less  than  four  feet.  Whether  this  was  due  to  defective 
tubing,  as  was  claimed,  could  not  be  ascertained. 

The  flowing  wells  at  Whitewater  are  confined  to  the  drift,  and  owe 
their  origin  to  the  fact  that  a.  bed  of  lacustrine  clay  rests  upon  the 
flank  of  drift  hills  to  the  southeast,  that  are  admirably  adapted  to 
serve  as  collecting  areas.  The  well  of  Mr.  P.  Dorr  is  52  feet  deep  in 
a  stiff  blue  clay.  Its  flow  is  copious  and  is  charged  with  iron  and 
sulphuretted  hydrogen. 

The  number  of  these  wells  may  be  somewhat  increased  in  all  prob 
ability,  but  the  limited  extent  of  the  clay  deposit  will  confine  then1 
to  the  localities  occupied  by  it. 

The  surface  of  the  Niagara  limestone  at  Manitowoc  is  thickly- 
covered  by  impervious  drift,  and  the  strata  beneath  rise  to  the  west- 
ward, and  are  partially  permeable  to  water,  so  that  the  requisite 
conditions  for  a  flowing  well  are  found  at  no  great  distance  within 
the  limestone,  if  the  boring  is  fortunate  in  striking  a  suitable  vein. 
A.t  the  well  of  Mr.  "William  Rahn,  the  drift  is  sixty  feet  deep  and  the 
rock  was  penetrated  ninety  feet.  The  wells  at  Washington  Park  and 
at  Woodman's  Tannery  are  given  as  about  the  same.  An  analysis  of 
the  water  of  Mr.  Rahn's  well  is  given  in  the  report  of  Dr.  Lapham, 
in  this  volume,  ante,  p,  31. 

The  following  section  of  the  well  at  Western  Union  Junction 
is  prepared  from  data  furnished  my  predecessor  by  John  C.  Gault, 
from  the  general  manager's  office  of  the  Milwaukee  &  St.  Paul  Rail- 
way Company,  to  whom  the  well  belongs.  This  and  the  following 
are  of  especial  interest  as  giving,  at  a  point  so  near  the  southeast  cor- 
ner of  the  state,  the  thickness  of  several  of  the  formations,  and  as 
furnishing  data  for  the  reliable  estimate  of  dip,  and  for  other  cal- 
culations : 


HYDROLOGY.  163 

Feet. 

Drift 147 

Niagara  limestone 233 

Cincinnati  shale 200 

Trenton  and  Galena  limestones 285 

St.  Peters  sandstone  (small  flow) 100 

Lower  Magnesian  limestone  141 

Potsdam  sandstone 157 


Total 1263 


The  record  says  that  fifteen  feet  of  limestone  were  passed  through 
in  this  lower  sandstone;  but  at  what  depth  is  not  stated.  It  also 
adds  that  red  rock  mingled  with  the  sand  from  below.  These  facts 
leave  no  doubt  that  this  is  the  Mendota  limestone,  which,  at  the 
typical  locality  near  Madison,  has  its  upper  surface  35  feet  below  the 
superior  face  of  the  sandstone. 

The  surface  of  this  well  is  144  feet  above  Lake  Michigan,  and  heiico 
its  bottom  is  541  feet  beneath  the  ocean  level.  The  water  rose  at  the 
time  of  drilling  to  the  height  of  40  feet  above  the  surface,  or  184  feet 
above  Lake  Michigan,  As  only  a  few  points  in  the  eastern  part  of  Ra- 
cine and  Kenosha  counties  exceed  that  elevation,  this  well  has  demon- 
strated the  possibility  of  obtaining  fountains  over  a  considerable  area. 

At  Racine  a  fine  flowing  well  has  recently  been  secured,  of  which 
Dr.  P.  R.  Hoy  has  kindly  furnished  me  the  data  which  show  the 

following  section: 

Feet. 

Drift 115 

Niagara  limestone 305 

Cincinnati  shale ,  •     185 

Galena  and  Trenton  limestones. . , 283 

St.  Peters  sandstone  48 

Lower  Magnesian  limestone 100 

Potsdam  group  — 

-Madison  sandstone 47     

Mendota  limestone 31     

Red  sandstone 110    ..    . 

Hard  sandstone 10     —  . 

Soft  sandstone  — 6     

204 


Total  depth 1240 


When  the  St.  Peter's  sandstone  was  reached,  a  flow  was  secured, 
which  was  increased  on  reaching  the  Madison,  and  still  further 
augmented  when  the  soft  sandstone  was  struck.  The  water  rose  in  a 
tube  65  feet  above  the  surface.  This  record  is  valuable  in  that  it 
demonstrates  the  existence  of  three  water-bearing  strata  above  the 
middle  Potsdam. 


164  GEOLOGY  OF  EASTERN  WISCONSIN. 

The  following  is  the  section  of  the  well  at  Milwaukee: 

Drift 170  feet. 

Niagara  limestone 267  " 

Cincinnati  shale 165  '• 

Trenton  and  Galena  limestones 253  " 

St.  Peters  sandstone 193  " 

1048  " 


The  surface  of  the  well  is  about  ten  feet  above  Lake  Michigan.  Its 
flow  is  strong  enough  to  fill  a  four-inch  pipe  at  sixty  feet  above  the 
surface.  From  the  pressure  at  the  surface,  it  was  estimated  by  the 
engineer  of  the  company  that  the  water  would  rise  100  feet  above  the 
surface,  or  110  feet  above  the  lake,  which  makes  it  probable  that  a 
similar  flow  might  be  obtained  at  other  localities  in  this  region  whose 
altitude  does  not  exceed  that.  By  consulting  the  table  of  elevations, 
it  will  be  seen  what  territory  is  included  in  this  limit. 

It  will  be  observed  that  this  flow  is  from  the  St.  Peters  sandstone. 
By  sinking  deeper  to  the  Potsdam,  a  vein  capable  of  rising  higher,  as 
at  Western  Union  Junction,  would  probably  be  reached. 

The  well  of  Sen.  "W.  H.  Jacobs,  in  the  suburbs  of  Milwaukee,  is  1,200 
feet  deep,  and  delivers  300  gallons  of  water  per  minute.  The  flow  may 
be  carried  over  50  feet  above  the  surface.  An  analysis  of  the  water 
by  Gustavus  Bode  shows  it  to  have  the  following  composition: 

Grains  in  1  gal.  U.  S.  measure. 

Chloride  of  potassium  0.2745 

Chloride  of  sodium „ . .  0.6405 

Sulphate  of  soda 8.8572 

Sulphate  of  lime 14.5485 

Bicarbonate  of  lime 8.6925 

Bicarbonate  of  magnesia 6.6307 

Bicarbonate  of  iron 0.1342 

Alumina 0. 1891 

Silica 2.3790 

Total 42.3462 

The  city  of  Sheboygan  has  recently  sunk  a  public  well  that  pos- 
sesses unusual  interest,  both  in  reference  to  the  strata  passed  through, 
and  the  character  of  the  water  obtained.  The  data  for  the  following 
section  were  furnished  through  the  courtesy  of  Mayor  George  End: 

Drift 92  feet. 

Niagara  limestone 719    ' 

Cincinnati  shale ..  .• 240    ' 

Trenton  and  Galena  limestones. , 213    ' 

St.  Peters  sandstone , , 212   ." 

Total..  1475    " 


HYDROLOGY.  165 

The  exact  depth  of  the  well  is  1,475  feet  and  4  inches.  At  the 
bottom,  a  very  hard  rock  is  said  to  have  been  struck,  which  was  be- 
lieved to  be  granite,  and  which  may  have  been  one  of  the  Archaean 
rocks,  as  they  rise  into  that  horizon  occasionally.  The  surface  of  the 
well  is  42  feet  above  Lake  Michigan;  its  bottom  855  feet  below  the 
ocean  level. 

Flowing  water  was  obtained  at  1,340  feet,  being  in  the  upper  por- 
tion of  the  St.  Peters  sandstone.  The  pressure  at  the  surface  is  suf- 
ficient to  raise  a  column  of  water  104  feet  above  the  surface,  or  146 
feet  above  the  lake,  which  differs  only  two  feet  from  that  obtained 
from  the  same  formation  at  Western  Union  Junction.  The  discharge 
of  water  is  225  gallons  per  minute.  Temperature,  59.1°  Fahr. 
Our  deep  seated  springs  range  from  47°  to  48°  Fahr.,  as  taken  in 
connection  with  field  work,  during  the  summer  season,  when  they 
would  be  warmest,  if  they  vary  at  all.  This  seems  to  show  that  the 
water  of  the  well  is  influenced  by  the  depths  from  which,  it  comes. 
The  following  is  an  analysis  of  the  water  by  Dr.  C.  F.  Chandler: 

Grains  per  U.  S.  Gallon. 

Chloride  of  sodium 306 . 9436 

Chloride  of  potassium 14.4822 

Chloride  of  lithium. 0. 1062 

Chloride  of  magnesium 54.9139 

Chloride  of  calcium 27.8225 

Bromide  of  sodium 0. 1873 

Iodide  of  sodium trace. 

Sulphate  of  lime 169.8277 

Sulphate  of  baryta trace. 

Bicarbonate  of  lime 13. 6585 

Bicarbonate  of  iron 0.5044 

'  Bicarbonate  of  manganese 0. 1742 

Phosphate  of  lime 0. 0383 

Biborate  of  soda trace. 

Alumina 0.1283 

Silica 0.4665 

Organic  matter   trace. 

Total 589.2536 


Density 1 .0093 


The  large  variety  and  quantity  of  salts  contained  in  this  water 
have  naturally  attracted  much  attention,  and  experience  will  doubt- 
less soon  demonstrate  the  specific  medicinal  effect  of  the  combination 
here  presented. 

At  first  thought  it  would  seem  not  a  little  remarkable  that  so  saline 
a  water  should  be  obtained  from  the  St.  Peters  sandstone,  a  formation 


166  GEOLOGY  OF  EASTERN  WISCONSIN. 

composed  almost  exclusively  of  quartzose  sand,  and  one  whose  waters 
elsewhere  contain  rather  less  than  the  usual  quantity  and  variety  of 
salts  found  in  our  native  waters.  But  we  must  consider  that  there  is 
here  a  depression  of  the  strata,  the  sandstone  being  here  lower  by  sev- 
eral hundred  feet  than  it  is  either  north,  south  or  west,  and  it  is  not 
known  to  outcrop  anywhere  to  the  eastward,  though  the  strata  above 
and  below  again  come  to  the  surface  in  Canada. 

The  facts  of  the  case  warrant  us  in  believing  that  there  is  no  escape 
for  the  waters  in  that  direction.  We  have  then  here  a  basin  reaching 
hundreds  of  feet  below  the  ocean  level.  Its  waters  have  no  outlet 
and  no  escape  except  'by  the  slow  process  of  diffusion  and  percolation 
through  almost  impervious  strata. 

That  the  water  should,  under  these  circumstances,  become  highly 
charged  with  saline  ingredients  is  not  at  all  remarkable,  though  the 
facts  are  of  an  exceedingly  interesting  nature. 

The  well  at  Janesville  is  located  upon  the  Fair  Grounds,  at  an  ele- 
vation of  about  295  feet  above  Lake  Michigan.  The  following  is  tho 
section  developed  by  an  examination  of  a  series  of  drillings  preserved 
by  Mr.  Cyrus  Miner,  to  whose  kindness  also  I  am  much  indebted  for 
other  information  relating  to  the  well: 

DRIFT. 

From  1  to  100  feet,  open  well  through  gravel. 
From  100  to  240  feet,  "  running  gravel." 

At  240  feet,  sand  and  gravel  of  drift  origin;  several  kinds  of  rock  represented. 
At  259  feet,  sand,  gravel  and  calcareous  clay. 
From  215  to  240  feet,  calcareous  arenaceous  clay. 

From  260  to  350  feet,  sand  and  gravel,  largely  quartz  and  chert,  a  little  granite,  dio- 
rite  and  some  limestone. 

POTSDAM. 

From  350  to  360  feet,  a  red  ocherous  material  mixed  with  a  nearly  equal  quantity  of 
green  particles  much  resembling  the  green  sand  of  the  Upper  Potsdam.  Drift  gravel, 
probably  from  above,  also  present.  The  red  and  green  mixture  effervesces  tardily  iu 
cold  acid  (hydrochloric),  but  very  briskly  in  hot,  showing  a  calcareous  and  magnesian 
element  present. 

At  390  feet,  light  colored  quartzose  and  cherty  sand,  with  a  few  granitic  and  calcare- 
ous grains. 

At  400  feet,  fine-grained  white,  chiefly  quartzose  sand,  but  indicating  the  presence  of 
calcareous  material  by  a  slight  effervescence  with  cold,  and  strong  action  with  hot  acid. 

At  450  feet,  essentially  the  same  as  above. 

At  515  feet,  quartzose  sand,  red  ocherous  material,  and  particles  of  a  purplish  shaly 
rock  partially  soluble  in  hydrochloric  acid. 

At  530  feet,  reddish  ocherous  material,  dark  calcareous  shale  and  small  drift  pebbles. 

At  565  feet,  greenish  blue  calcareous  shale  containing  minute  glistening  scales  re- 
sembling mica. 

From  560  to  570  feet,  similar  to  the  last. 

At  615  feet,  fine  grained  light  yellow  quartzose  sand;  slight  effervescence. 


HYDROLOGY.  167 

At  680  feet,  fine  grained  white  quartzose  sand;  slight  effervescence. 

At  640  feet,  fine  grained  quartzose  sand,  with  slightly  reddish  clay-like  calcareous 
material. 

At  710  feet,  fine  grained,  light  colored,  quartzose  sand;  slight  effervescence. 

At  758  feet,  rather  coarse,  white  and  slightly  greenish  quartzose  sand,  with  a  little 
clayey  material;  no  effervescence. 

At  940  feet,  coarse  white  quartzose  sand. 

At  975  feet,  similar  to  above,  but  coarser. 

At  1022  feet,  very  coarse,  transparent  quartz  sand,  some  of  the  grains  one-sixth  of  an 
<nch  in  diameter. 

Bottom,  1033  feet. 

STJMMAKY. 

Drift 360  feet. 

Red  and  green  rock,  probably  Mendota  horizon 10 

Fine  grained,  slightly  calcareous  sandstone 155 

Calcareous  shale 80 

Fine  grained,  very  slightly  calcareous  sandstone 163 

Coarse  non-calcareous  sandstone 275 

Total 1033    " 

Drift,  350  feet.    Postdam,  683  feet. 

Probably  40  to  50  feet  of  the  upper  portion  of  the  Potsdam  has 
been  removed,  making  the  thickness  about  725  feet,  with  the  bottom 
not  reached. 

In  the  upper  portion  of  the  Potsdam  horizon,  a  vein  was  struck 
which  gave  a  permanent  rise  in  the  tube  of  48  feet  above  the  water 
level  in  the  open  well,  without  the  aid  of  a  seed-bag  or  other  appara- 
tus for  preventing  lateral  leakage.  This  corresponds,  according  to 
aneroid  measurement,  to  •  147  feet  above  Lake  Michigan,  or  7  feet 
above  the  depot  at  Janes ville. 

The  unusual  thickness  of  the  drift  is  probably  due  to  an  old  pre- 
glacial  caflon  of  Rock  river,  now  filled,  as  the  full  series  of  formations, 
up  to  the  Trenton  limestone,  occurs  on  the  opposite  side  of  the  river, 
and  also  at  a  short  distance  to  the  east.  The  circumstances  that  ne- 
cessitated the  selection  of  the  fair  grounds  for  this  test  well  are  to  be 
regretted,  since  at  the  locality  for  which  my  estimate  was  given,  the 
exceptional  difficulties  with  the  drift  would  not  have  been  encoun- 
tered, and  a  satisfactory  flow  would  undoubtedly  have  been  obtained. 
Nevertheless,  through  the  enterprise  and  ingenuity  of  the  parties  hav- 
ing the  matter  in  hand,  a  success  scarcely  less  satisfactory  has  been 
attained.  Advantage  has  been  taken  of  the  rise  of  48  feet  in  the  tube 
above  that  in  the  well,  to  raise  a  portion  of  the  generous  flow  to  the 
surface  by  hydraulic  appliances. 

Possibilities  of  obtaining  wells  at  other  points.  Reference  has 
been  had  to  this  important  practical  question  in  the  foregoing  des- 


168  GEOLOGY  OF  EASTERN  WISCONSIN. 

criptions,  and  in  the  subsequent  treatment  of  the  geological  series, 
large,  and  it  is  hoped  ample  contributions  will  be  made  to  it,  though 
it  will  not  be  always  specifically  designated,  as  that  would  burden  the 
report  to  the  exclusion  of  other  valuable  matter.  Special  estimate 
should  be  made  for  every  locality  before  commencing  to  sink  an  ex- 
pensive well,  as  there  are  often  local  elements  that  enter  into  the  prob- 
lem and  determine  success  or  failure.  It  needs  also  to  be  borne  in 
mind  that  even  in  a  favorable  locality,  failure  may  result,  as  the  strata 
are  not  uniformly  porous,  and  it  is  possible  to  bore  through  a  forma- 
tion that  is  in  most  parts  highly  water-bearing,  without  striking  a 
vein  or  seam.  Only  a  single  marked  instance  of  this,  however,  has 
come  to  my  notice.  Failure,  also,  often  results  from  not  properly 
controlling  the  water,  ~by  the  intelligent  use  of  tube  and  seed-bag,  or 
equivalent  apparatus,  and  by  failure  to  recognize  a  suitable  vein  when 
reached.  These  and  other  matters  will  be  found  more  fully  discussed 
in  the  general  article  on  the  subject  in  Volume  I. 

Bearing  these  points  in  mind,  and  leaving  out  of  consideration  the 
drift  system  of  wells  which,  from  their  superficial  character  and  the 
nature  of  the  formation,  have  only  a  local  importance,  there  are  three 
extensive  areas  over  which  there  is  a  reasonable  presumption  that 
fountains  may  be  obtained. 

The  first  is  a  belt  adjoining  Lake  Michigan.  Where  the  elevation 
is  but  a  few  feet  above  the  lake  surface,  streams  will  be  found,  in  some 
cases,  in  the  Niagara  limestone,  which,  if  intelligently  controlled,  will 
furnish  a  flow  at  the  surface.  This  source  will  be,  however,  uncer- 
tain. But  by  penetrating  to  the  St.  Peters  sandstone,  the  probabili- 
ties- of  success  will  be  large,  and  they  will  be  reinforced  by  the  chances 
lying  in  the  Potsdam  sandstone  below,  though  the  depth  of  this 
will  be  considerable.  Near  the  lake  level,  the  chances  from  these 
sources  will  be  good  for  the  whole  of  the  lake  border.  From  Mani- 

O 

towoc  county  southward,  they  may  be  said  to  hold  good  for  elevations 
not  exceeding  100  feet  above  the  lake,  and  to  be  fair  up  to  140  feet, 
but  slight  above  150  feet,  though  perhaps  possible  in  some  locations 
at  200  feet  or  more. 

The  elevations  previously  given  in  this  report,  and  the  topographi- 
cal map  will  show  what  localities  fall  within  the  limits  of  these  con- 
ditions. The  facts  connected  with  the  wells  already  described,  and 
the  data  given  in  relation  to  the  several  formations,  will  permit  an  ap- 
proximate calculation  of  the  depth,  nature  of  the  drilling,  and  conse- 
quent cost. 

The  second  area  consists  of  the  Green  Bay  valley,  from  Fond  du 
Lac  northward.  In  the  vicinity  of  Lake  "Winnebago,  a  flow  from 


HYDEOLOGY.  109 

either  the  St.  Peters  or  Potsdam  sandstones  can  not  be  relied  upon  at 
an  elevation  exceeding  15  feet  above  the  lake  surface,  though  Mr. 
"Wild's  well  has  demonstrated  that  it  is  possible  at  50  feet.  On  the 
other  hand,  however,  the  wells  at  Oshkosh  show  that  the  limit  given 
is  the  extreme  one  that  is  reasonably  trustworthy. 

To  the  north  of  Lake  Winnebago  the  limit  in  altitude  descends  at 
about  the  same  ratio  as  the  general  surface  of  the  valley.  It  must 
be  remembered,  however,  that  the  St.  Peters  sandstone  is  not  so  relia- 
ble in  this  region  as  farther  south,  where  its  thickness  is  more  uni- 
form. The  Potsdam  sandstone  should,  however,  present  reasonable 
probabilities  for  the  region  along  the  Bay,  at  elevations  not  exceeding 
25  or  30  feet  above  its  surface,  with  slight  chances  for  greater  alti- 
tudes. 

The  third  district  lies  in  the  valley  of  Rock  river.  An  elevation 
of  250  feet  must  be  taken  as  the  upper  limit  of  favorable  chances. 
That  a  flow  at  this  altitude  is  attainable  is  shown  by  the  wells  at 
Watertown,  Palmyra  and  Janesville.  The  St.  Peters  sandstone  is 
available  for  only  a  portion  of  the  area  that  falls  below  that  altitude, 
since  in  some  parts  of  it,  this  formation  is  deeply  eroded  by  the 
streams,  and  its  fountain-forming  possibilities  destroyed.  Success  in 
these  portions  will  be  chiefly  dependent  on  the  Potsdam  sandstone. 

The  list  of  elevations  and  the  maps  will  be  found  indispensable  to 
an  intelligent  calculation  of  probabilities  in  this  region,  and  something 
more  than  wonted  caution  may  here  be  recommended,  because  of  the 
nature  of  the  formations,  their  nearness  to  the  central  anticlinal  axis 
of  the  state,  and  the  presence  of  deep  ancient  river  gorges  now  filled 
and  concealed  by  drift. 

As  the  majority  of  the  deep  seated  wells  of  eastern  Wisconsin  de- 
rive their  flow  from  the  St.  Peters  sandstone,  it  is  important  to  know 
at  what  elevation  the  upper  face  of  that  formation  outcrops.  The  fol- 
lowing list  will  supply  the  requisite  data: 

ELEVATIONS  OF  THE  JUNCTION  OF   THE  ST.  PETERS  SANDSTONE  AND  TRENTON 

LIMESTONE. 


Rock  County. 

Avon  —  Feet. 

Sec.   5,  N.  E.  qr.,           -  -    272 

9,         -           -  -           250 
Beloit  — 

Sec.  3,  S.  W.  qr.,  -    229 

3,  S.  W.  qr.ofS.  W.  qr.,        196 

10,  N.  E.  qr.,            -  -     180 

10,  S.  E.  qr.,         -  -            200 

Fulton  — 

Sec.  10,  S.  W.  qr.,           -  -    219 

Newville  bridge,  Eock  river,  -           208 


Rock  County —  (con.) 

Magnolia  —  Feet- 

Sec.    6,  S.  W  qr.,  -    309 

7,  S.  E.  qr.,     -  -            433 

28,  S.  W.  qr.,  -            -    339 

R.  E.  cut,  330 
Porter  — 

Sec.  9,  N.  W.  qr.,  -    250 
Eock  — 

Sec.  32,  189 

Alton,     -           -  -           -    208 


1TO 


GEOLOGY  OF  EASTERN  WISCONSIN. 


ELEVATIOXS,  etc.  —  continued. 


Rock  County  —  (con.) 

Spring  Valley  —  Feet. 

Sec.    3,  S.  W.  qr.  of  S.  W.  or.,       314 

4,     -            -  -            -    338 

9,  center,  321 

13,  mid.  N.  line,  -            -    300 

15,  S.  E.  qr.,     -  -           321 
28,  N.  E.  qr.,  -            -    296 
33,  S.  E.  qr.,     -  268 

Union  — 

Sec.  12,  near  center,  -           -    298 
Jefferson  County. 
Lake  Mills  — 

Sec.  3,  N.  W.  qr.,  -           -    319 

4,  N.  W.  qr.,  -           330 
Milford  — 

Sec.    7,  S.  W.  qr.,  -            -    251 

33,  N.  E.  qr.  (est.),  -           257 
Oakland  — 

Sec.  18,  S.  E.  qr.,  -    246 

16,  N.  W.  corner,  -            264 
28,  mid.  E.  line  (est),  -    233 

Sec.  30,  N.  W.  qr.,  -           253 
Sumner  — 

Sec.  18,  (est.),      -  -           -    202 
Waterloo  — 

Sec.  31,  county  line  (est),     -  323 

35,  S.  E.  qr.  (est.),  -           -    277 
Dane  County  — 
Christiana  — 

Sec.  24,  N.  hf  (est.),  261 
Medina  — 

Sec.  25,  E.  hf  (near),  -           -    331 


Dane  County  —  (con.) 
Rutland  —  Feet. 

Sec.  34,  S.  E.  qr.,    -  -  348 

Dodge  County. 
Elba  — 

Sec.  25,  (very  near),        -  -    254 

Fox  Lake  — 

Sec.  17,  S.  E.  qr.,    -  294 

31,  N.  W.  qr.   of  N.   W.  qr. 

(est.),     -  -    368 

31,  mid.  W.  line  N.  W.  qr.,    329 
Lowell  (T.  10,  R.  14)  — 

Sec.  19  (est.),       -  -    195 

Portland  — 

Sec.    6,  N.  W.  qr.,  -    296 

31,  -  -  248 

Shields  — 

Sec.  32  (near),     -  -    214 

Westford  (T.  12,  R.  13)  — 

Sec.  25,    -  -    2GC 

Fond  du  Lac  County. 
Metomen  — 
Sec.  31,  S.  W.  corner,    -  -    412 

Ripon  — 

city,  30  rods.  W.  of  P.  0.  (near)  381 

city,  falls  under  tressel  bridge,  333 

W.  of  city,  -  414 

Sec.  20,  N.  W.  qr.  of  N.  W.  qr.,  328 

20,  little  W.  of  center,         -  297 

21,  S.  E.  qr.  of  S.  W.  qr.,  364 
29,  N.  E.  qr.,     -  350 
29,  E.  hf,  valley,      -           -  341 


Those  marked  estimated,  or  near,  are  cases  in  which  the  actual  junction  was  not  seen^ 
but  was  calulated  from  the  thickness  of  the  Trenton  limestone  above. 

Water  Power.  The  great  interior  and  the  west  are  laboring  un- 
der a  serious  error  which  intelligent  action  may  remove.  They  pro- 
duce vast  quantities  of  crude  material  needing  manufacture.  This 
bulky  and  heavy  matter  they  transport  a  thousand  miles  to  be  worked 
up.  They  likewise  produce  immense  quantities  of  food.  This  they 
carry  the  same  thousand  miles  to  feed  those  who  manufacture  the 
other  material.  They  then  bring  back  the  manufactured  article  mur- 
muring at  its  expense  and  praying  for  cheap  transportation.  More 
simply  and  truly  stated,  the  situation  is  this:  At  one  end  of  a  thous- 
and miles  is  a  man  and  his  tools;  at  the  other  end  is  the  heap  of  the 
crude  material  he  is  to  manufacture,  the  bulky  food  he  is  to  eat,  and 
the  market  for  his  products ;  and  the  problem  is,  Shall  the  mountain 
ero  to  Mohammed  or  will  Mohammed  come  to  the  mountain?  An 

o 

intelligent  practical  answer  to  this  will  go  some  way  toward  solving 
the  problem  of  cheap  transportation.  Agriculture,  mining,  and  man- 
ufacture form  a  triangle  of  industries  that  are  mutually  dependent,  and 
the  nearer  they  can  be  brought  together  the  more  successful  will 
each  be. 


HYDROLOGY.  171 

The  question  then,  "What  facilities  for  manufacturing  does  our  state 
present?  becomes  one  of  the  highest  importance,  especially  so  to  our 
preponderating  agricultural  interests.  Chief  among  these  is  water 
power. 

In  the  district  ur.der  consideration  there  is  a  vast  amount  of  water 
power  situated  in  the  heart  of  an  exceedingly  rich  farming  country, 
with  abundant  facilities  for  transportation,  and,  not  by  any  means  a 
subordinate  consideration,  in  the  midst  of  an  intelligent,  cultured  so- 
ciety. The  object  of  this  chapter  will  be  to  give  trustworthy  facts  for 
the  guidance  of  capitalists,  who  may  have  the  prescience  to  foresee 
that  the  natural  facilities  for  manufacturing  in  the  interior  must  in 
the  immediate  future  be  utilized  to  their  utmost  capacity  and  must 
become  correspondingly  valuable. 

Water  Power  of  Rock  river.  For  a  portion  of  the  facts  here 
given,  credit  is  due  the  report  of  Brevet  Maj.  Gen.  James  H.  Wilson, 
on  the  survey  of  Rock  river,  under  the  direction  of  the  U.  S.  Engi- 
neer Department,  and  for  another  portion  to  a  very  careful  survey  of  the 
lower  portion  of  the  river  by  Edward  Ruger,  C.  E.,  made  to  deter- 
mine the  availability  of  Lake  Koshkonong  as  a  storage  reservoir.  I 
am  indebted  for  the  use  of  the  latter  to  the  kindness  of  J.  M.  Cobb, 
Esq.,  through  whose  efforts  the  enterprise  has  been  brought  to  a  suc- 
cessful issue.  The  remaining  data  have  been  gathered  during  the 
progress  of  the  present  survey. 

The  entire  area  drained  by  Rock  river  and  its  tributaries  in  Wis- 
consin is  3,635  square  miles.  From  the  Table  of  Rainfall  at  Milwau- 
kee, given  in  Dr.  Lapham's  report,  this  volume,  it  appears  that  the 
average  rainfall  for  the  past  thirty  years  is  30.27  in.,  which  may  be 
assumed  as  at  least  approximately  correct  for  the  Rock  river  valley. 
The  average  fall  for  some  portions  of  Wisconsin  is  given  in  Gen. 
Humphrey's  work  on  the  hydraulics  of  the  Mississippi  at  35  inches. 
But  reckoning  at  30  inches,  the  rainfall  upon  the  drainage  area  under 
consideration  would  be  253,344,960,000  cubic  feet.  Now  it  is  asserted 
by  varidus  authorities,  based  on  experience,  that  one-half  the  rainfall 
can  be  utilized.  This  would  give  126,672,480,000  cubic  feet  per  an- 
num. Mr.  Ruger  says:  "From  personal  observations,  and  after  con- 
sulting many  authorities  as  to  rainfall,  springs,  evaporation,  filtration, 
etc.,  I  estimate  that  the  total  annual  quantity  of  water  passing  in 
Rock  river  at  the  state  line,  including  Turtle  Creek,  is  98,4-37,536,000 
cubic  feet,"  which  may  be  regarded  as  a  safe  estimate.  The  daily 
supply,  by  this  estimate,  would  be  269,691,879  cubic  feet.  We  need 
next  to  ascertain  what  is  the  average  descent  of  this  volume.  Some 
of  it  falls  over  600  feet,  while  other  portions  practically  no  distance. 


172  GEOLOGY  OF  EASTERN  WISCONSIN. 

The*  average  elevation  of  the  rim  of  the  basin  above  the  point  where 
the  river  leaves  the  state  is  about  250  feet,  its  average  distance  about 
50  miles,  showing  an  average  fall  of  about  five  feet  per  mile.  But 
this  is  less  to  the  point  than  the  following. 

The  average  elevation  of  fifteen  powers,  the  first  of  importance  on 
their  respective  branches  is  about  155  feet  above  the  surface  of  the 
river  where  it  leaves  the  state  at  Beloit.  The  average  fall  from  these 
powers  to  the  state  line  is  a  little  less  than  three  feet  per  mile. 

With  these  general  statements,  we  will  set  aside  the  tributaries, 
several  of  which  are  important,  and  consider  more  accurately  the 
main  stream  between  Horicon  and  Beloit.  The  collecting  area  above 
Horicon  is  436  square  miles,  upon  which  the  annual  rainfall,  reckoned 
at  thirty  inches,  would  be  80,887,456,000  cubic  feet.  Allowing  one- 
half  for  evaporation,  filtration,  and  other  sources  of  loss,  the  theoretical 
discharge  at  the  outlet  of  Horicon  marsh  would  be  15,193,728,000 
cubic  feet.  Reckoned  at  the  lowest  rainfall  in  the  last  thirty  years, 
the  amount  would  be  10,114,749,120  cubic  feet.  Col.  Worrall  gives 
in  the  report  previously  referred  to,  as  the  result  of  a  careful  meas- 
urement of  the  flow  at  a  time  when  the  volume  was  estimated  to  be 
only  three-fourths  of  the  average,  a  supply  of  27,651  cubic  feet  per 
minute,  or  14,533,365,600  cubic  feet  per  annum,  from  which  it  would 
seem  that  the  calculated  amount  is  not  far  from  the  truth.  From 
the  foregoing  data,  estimating  the  accession  from  tributaries,  it  is 
thought  to  be  safe  to  consider  the  average  flow  between  Horicon  and 
Beloit  as  in  round  numbers  50,000,000,000  cubic  feet  per  annum. 
The  fall  from  Horicon  to  the  state  line  is  127  feet.  An  estimate  of 
the  theoretical  power  generated  by  the  main  river  shows  it  to  be  up- 
wards of  20,000  horse  power.  Of  the  127  feet  fall,  less  than  60  feet 
are  utilized.  Of  the  unused  portion  there  is  more  than  30  feet  fall 
between  Horicon  and  Watertown,  corresponding  to  above  1,600  horse 
power,  and  about  23  feet  fall  between  Janesville  and  Beloit,  equal  to 
upwards  of  7,000  horse  power.  A  portion  of  this  latter^  may  readily 
be  made  available  at  Beloit  by  means  of  a  race  leading  from  a  dam 
situated  above  the  slack  water  of  the  present  one.  Another  power 
near  the  state  line  can  also  be  utilized  to  the  profit  of  this  place. 
Upon  the  river  and  its  tributaries  are  a  large  number  of  lakes  that 
may  be  utilized  as  storage  reservoirs,  thus  affecting  a  much  greater 
economy  in  the  use  of  the  water. 

Water  power  of  the  Fox  river.1     The  upper  Fox  river  from  its 

1  For  the  leading  facts  here  given,  I  am  indebted  to  an  article  prepared  for  the  Cen- 
tennial Commission  by  Pres.  G.  M.  Steele,  of  Lawrence  University.  I  am  also  indebted 
to  Prof.  J.  C.  Foye  of  the  same  institution  for  similar  favors. 


HYDROLOGY.  173 

slight  descent  furnishes  no  water  power,  a  fact  which  is  compensated 
for  by  the  facilities  it  offers  for  navigation.  But  the  lower  Fox  river 
presents  an  almost  continuous  series  of  rapids  from  Lake  Winnebago 
to  Green  Bay.  In  this  distance  of  about  thirty-five  miles  it  has  a 
fall  of  170  feet,  so  distributed  as  to  be  completely  and  economically 
utilized.  The  powers  upon  this  river  possess  an  immense  advantage 
in  the  grand  natural  reservoir  furnished  by  lake  Winnebago,  which 
embraces  an  area  of  about  350  square  miles.  Neither  floods  nor 
drouth  cause  any  considerable  or  inconvenient  fluctations  in  its  level, 
and  the  steady  reliable  flow  thus  secured  at  all  seasons  is  a  vast  ad- 
vantage. The  channel  of  the  river  consists  of  a  gorge  between  clay 
banks,  with  a  floor  of  heavy  bedded  limestone,  so  that  it  may  be 
dammed  with  material  taken  from  its  own  bed,  and  without  overflow- 
ing adjacent  lowlands.  The  great  reservoir  makes  it  unnecessary  to 
have  more  than  a  limited  local  one,  sufficient  to  guard  against  inter- 
ference from  other  powers. 

The  minimum  flowage  is  estimated  at  150,000  feet  per  second,  this 
amount  being  available  at  all  seasons  of  the  year.  The  height  and 
power  of  the  several  falls  estimated  on  this  basis  are  as  follows: 

Names  of  places.     ,                                                 Height  of  fall.  Horse  power. 

Neenali  and  Menasha 10  3,000 

Appleton 38  11,500 

Cedars 10  3,000 

Little  Chute 38  11,500 

Kaukauna 40  14,500 

Rapid  Crosche 8  2,300 

Little  Kaukauna 8  2,300 

DePere .'  8  2,300 

Total 150  50,400 


At  Neenah,  Menasha,  Appleton  and  De  Pere,  a  considerable  per- 
centage of  the  power  is  now  utilized,  though  a  large  amount  is  still 
unimproved,  particularly  at  Appleton.  But  at  the  other  points  only 
the  merest  fraction  is  now  used,  and  a  wealth  of  power  remains  unoc- 
cupied. Attention  has  already  been  called  to  the  facilities  for  trans- 
portation available  to  manufacturers  in  this  valley,  and  by  consulting 
subsequent  portions  of  this  report  it  will  be  seen  that  the  agricultural 
and  other  industrial  capabilities  of  the  adjacent  and  tributary  regions 
are  very  great. 

On  the  upper  portions  of  the  Wolf,  Oconto,  Peshtigo  and  Menom- 
onee  rivers  are  numerous  falls  and  rapids  furnishing  immense  power, 
but  these  lie  chiefly  beyond  the  limits  of  the  district  under  descrip- 
tion. The  falls  of  the  Oconto,  however,  where,  by  including  the  rapids 


174  GEOLOGY  OF  EASTERN  WISCONSIN. 

above  and  below,  a  descent  of  about  60  feet  may  be  made  available, 
and  the  lower  rapids  on  the  Peshtigo  and  Menomonee  lie  within  our 
province  and  also  within  the  limits  of  settlement,  and  mast,  in  the  not 
distant  future,  be  improved. 

On  the  Lake  Michigan  slope  all  the  available  power  must  soon  be 
called  into  use  by  the  rapid  development  of  that  region. 

The  average  height  of  the  watershed  is  over  300  feet,  and  its  aver- 
age distance  from  the  lake  less  than  30  miles,  giving  a  fall,  if  a  direct 
course  to  the  lake  were  pursued,  of  more  than  10  feet  per  mile.  Or 
to  put  it  in  a  more  utilitarian  form,  a  dam  might  be  constructed  at 
the  end  of  every  mile,  having  a  fall  of  eight  feet,  and  still  leave  de- 
scent enough  to  cause  a  rapid  flow.  The  crooked  course  of  the  rivers 
however  very  much  reduces  the  rapidity  of  descent. 

The  Milwaukee  river  is  first  utilized  as  a  water  power  at  a  height 
of  about  475  feet  above  Lake '  Michigan.  At  Barton  it  has  become  a 
very  considerable  stream,  and  is  still  311  feet  above 'the  lake  level. 
Between  "West  Bend  and  its  mouth,  it  has  a  fall  of  295  feet.  If  it 
pursued  a  direct  course  to  the  lake,  it  would  have  a  fall  of  16£  feet  to 
the  mile.  If  it  pursued  a  direct  course  to  its  mouth,  it  would  have  a 
fall  of  9£  feet  to  the  mile.  As  it  is,  notwithstanding  its  tortuous 
course,  it  has  an  average  fall,  as  nearly  as  I  can  estimate  it,  of  five 
feet  per  mile.  A  portion  of  the  power  thus  given  is  not  yet  im- 
proved. 

The  Sheboygan  river  is  utilized  at  a  height  of  about  320  feet,  and 
is  capable  of  affording  an  extensive  reservoir  at  that  elevation. 

The  Manitowoc  is  a  very  considerable  stream  at  an  elevation  of  275 
feet,  and  has  a  very  rapid  descent  in  the  lower  half  of  i£s  course. 

Many  of  the  smaller  streams  also  furnish  efficient  water  power. 

Changes  in  Drainage.  A  comparison  of  the  streams  and  smaller 
marshes,  as  laid  down  on  the  government  plats  and  earlier  maps,  with 
the  present  facts  show  important  changes  in  the  drainage  of  the  re- 
gion. Large  areas  that  are  represented  as  marsh  on  the  plats  of  the 
government  survey  are  now  comparatively  dry  and  arable.  Many  of 
the  smaller  streams  have  disappeared  or  become  mere  periodical  runs. 
On  the  accompanying  maps  the  areas  laid  down  as  marsh  by  the 
original  govenment  survey  have  been  indicated  with  such  correc- 
tions as  could  be  made.  They  are,  however,  designated  as  wet  lands, 
since  a  large  part  are  not  now  really  marsh,  and  indeed  a  portion  is 
cultivated  in  all  but  very  wet  seasons.  They  are  as  a  class  among 
the  most  valuable  lands  in  the  state.  The  mapping  of  these  areas, 
besides  being  valuable  as  topographical  and  geological  data,  has  a  his- 
torical significance;  since  it  shows  what  was  regarded  as  marshy  at 


HYDROLOGY.  175 

the  time  of  the  government  survey,  and  thereby  indicates  the  changes 
that  have  since  ensued.  These  changes  have  been  much  more  marked  in 
the  forest  regions  than  in  the  more  open  country,  and  are  so  intimately 
connected  with  the  clearing  away  of  the  timber  that  it  is  a  fair  infer- 
ence that  this  is  the  main  cause. 

The  timber  is  often  very  heavy,  and  consequently  permits  but  a 
very  feeble  undergrowth.  The  removal  of  the  original  forest  thus 
leaves  the  surface  almost  entirely  bare,  and  it  is  usually  at  once  put 
under  cultivation.  The  effect  of  so  great  a  change  would  naturally 
make  itself  felt  upon  the  drainage  of  the  region.  To  the  extent  to 
which  this  has  gone  thus  far,  it  has  doubtless  on  the  whole  been  a 
benefit  to  the  region,  as  it  has  induced  a  drier,  lighter,  warmer  soil, 
and  more  healthful  atmosphere.  But  the  limit  of  benefit  in  this  di- 
rection may  be  assumed  to  have  been  reached  except  in  certain  locali- 
ties, and  the  danger  now  to  be  apprehended  is  that  it  will  proceed  to 
an  injurious  extent.  This,  however,  can  easily  be  avoided,  if  clearly 
foreseen  and  justly  appreciated. 


176  GEOLOGY  OF  EASTEEN  WISCONSIN. 


CHAPTER  III. 
NATIVE    YEGETATIOK 

The  most  reliable  natural  indications  of  the  agricultural  capabilities 
of  a  district  are  to  be  found  in  its  native  vegetation.  The  natural 
flora  may  be  regarded  as  the  result  of  nature's  experiments  in  crop 
raising  through  the  thousands  of  years  that  have  elapsed  since  the  re- 
gion became  covered  with  vegetation.  If  we  set  aside  the  inherent 
nature  of  the  several  plants,  the  native  vegetation  may  be  regarded  as 
the  natural  correlation  of  the  combined  agricultural  influences  of  soil, 
climate,  topography,  drainage  and  underlying  formations  and  their 
effect  upon  it.  To  determine  the  exact  character  of  each  of  these 
agencies  independently  is  a  work  of  no  little  difficulty;  and  then  to 
compare  and  combine  their  respective  influences  upon  vegetation  pre- 
sents very  great  additional  difficulty.  But  the  experiments  of  nature 
furnish  us  in  the  native  flora  a  practical  correlation  of  them.  Tho 
native  vegetation  therefore  merits  careful  consideration,  none  the  less 
so  because  it  is  rapidly  disappearing,  and  a  record  of  it  will  be  valua- 
ble historically. 

It  is  rare  in  nature  that  a  single  plant  occupies  exclusively  any  con- 
siderable territory,  and  in  this  respect  there  is  an  important  difference 
between  nature's  methods  and  those  of  man.  The  former  raises  mixed 
crops,  the  latter  chiefly  simple  ones.  But  in  nature,  the  mingling  of 
plants  is  not  miscellaneous  or  fortuitous.  They  are  not  indiscrimi- 
nately intermixed  with  each  other  without  regard  to  their  fitness  to  be 
companions,  but  occur  in  groups  or  communities,  the  members  of  which 
are  adapted  to  each  other  and  to  their  common  surroundings.  It  be- 
comes then  a  question  of  much  interest  and  of  high  practical  import- 
ance to  ascertain,  within  the  region  under  consideration,  what  are  the 
natural  groupings  of  plants,  and  then  what  areas  are  occupied  by  the 
several  groups,  after  which  a  comparison  with  the  soils,  geological 
formations,  surface  configuration,  drainage  and  climatic  influences 
cannot  fail  to  be  productive  of  valuable  results. 

The  following  natural  groups  are  usually  well  marked,  though  of 
course  they  merge  into  each  other  where  there  is  a  gradual  transition 
from  the  conditions  favorable  for  one  group,  to  those  advantageous  to 
another.  In  some  instances  it  is  unquestionably  true  that  other  cir- 


NATIVE  VEGETATION.  177 

cum  stances  than  natural  adaptabilities  control  the  association  of  these 
plants,  and  an  effort  has  been  made  in  the  study  of  the  region,  to  dis- 
cern these  cases  and  eliminate  them  from  the  results,  so  that  the 
groups  which  are  here  given  are  believed  to  be  natural  associations  of 
plants.  Their  distribution  is  held  to  show  in  what  localities  condi- 
tions peculiarly  advantageous  to  them  occur,  and  hence  advantageous 
to  those  cultivated  plants  that  require  similar  conditions. 

A.    UPLAND  VEGETATION. 

(1)  Herbaceous. 

CLASS  I.  Prairie  Group.  One  of  the  most  natural  and  sharply 
defined  groups  is  constituted  by  our  prairie  vegetation.  It  differs 
from  all  other  groups  that  grow  upon  the  uplands,  in  being  almost 
exclusively  herbaceous,  and  in  the  fact  that  the  species  composing  it, 
more  rarely  intermingle  with  the  other  groups.  It  is  more  distinct 
from  them  than  they  are  from  each  other,  and  justifies  the  division 
of  the  upland  flora  into  prairie  and  forest  vegetation.  Its  characteris- 
tics are  too  well  known  to  need  further  definition  here. 

(2)  Arboreous. 

CLASS  II.  The  Oak  Group.  This  is  most  nearly  related  to  and 
most  closely  associated  with  the  prairie  group.  The  prairies  are  rarely 
contiguous  to  any  other  form  of  arboreous  vegetation. 

The  Burr  Oak  (Quercus  macrooarpa),  the  White  Oak  (Quercus  alba\ 
the  Red  Oak  (Quercus  rubra\  the  Pin  Oak  (Quercus  palustris\  are 
the  most  prominent  species,  and  give  name  to  the  whole.  The  Chest- 
nut Oak  (Quercus  prinus)  is  associated  with  these  just  north  of  Janes- 
ville,  but  I  have  observed  it  at  no  other  point  within  the  state.  The 
common  Poplar  or  Aspen  (Populus  tremuloides)  is  the  most  con- 
spicuous associate  of  these  oaks,  but  it  is  not  confined  to  this  associa- 
tion. The  Large-toothed  Poplar  (Populus  grandidentata)  is  some- 
times found  with  this  group,  but  much  prefers  association  with  the 
maples.  This  and  the  preceding  species  are  in  a  sense  the  comple- 
ments of  each  other.  Those  associations  that  are  avoided  by  the  one 
are  sought  by  the  other,  though  they  not  unfrequently  mingle.  The 
Populus  balsamifera  and  P.  candicans  have  not  been  observed  min- 
gling with  this  group.  The  Shell-bark  Hickory  (Carya  alba)  is  an- 
other prominent  member  of  this  cluster.  The  Pignut  Hickory  (Carya 
glabra)  is  occasionally,  but  not  frequently  found  in  this  group.  It 
sustains  the  same  relation  to  the  Shell-bark  Hiakory  tl  at  the  Great- 
toothed  Poplar  does  to  the  Trembling  Aspen.  The  Crab  Apple  (Py- 
Wis.  SUR.  — 12 


178  GEOLOGY  OF  EASTERN  WISCONSIN. 

rus  coronaria),  the  "Wild  Black  Cherry  (Prunus  serotina),  the  Choke 
Cherry  (Prunus  Virginiana),  and  the  Wild  Plum  (Prunus  Ameri- 
cana), represent  the  Rosacese.  The  Sumac  (Rhus  typhina)  is  com- 
mon, but  not  significant,  as  it  is  a  member  of  other  groups. 

The  attendant  underbrush  is  equally  characteristic.  The  Hazel- 
nut  (Corylus  Americana)  is  almost  everywhere  present  with  this 
group,  though  rare  or  wanting  in  connection  with  the  others.  The 
Panicled  Cornel  (Cornus  paniculata)  is  very  common,  and  with  the 
Hazel  constitutes  the  chief  underbrush.  The  Wild  Red  and  Black 
Raspberries  (Rubus  strigosus  and  occidentalis)  and  the  High-bush 
Blackberry  (Rubus  villosus)  are  all  present,  but  seem  to  prefer  asso- 
ciation wTith  the  other  groups. 

If  we  descend  to  the  herbaceous  vegetation  beneath,  similar  facts 
will  be  found,  but  it  would  transcend  the  brevity  desirable  in  this 
report  to  enter  fully  into  the  details.  And  there  is  this  further  rea- 
son for  not  doing  so  in  this  connection,  that  many  of  these  plants  are 
more  dependent  upon  the  conditions  furnished  by  the  overshadowing 
vegetation,  than  upon  the  nature  of  the  soil,  and  are  therefore  less 
instructive  as  to  agricultural  questions. 

This  group  as  here  constituted  includes  both  the  "  Oak  openings" 
or  "  Oak  orchards,"  and  the  denser  oak  forests.  There  are  sufficient 
reasons,  however,  for  separating  them  into  two  classes,  as  they  indi- 
cate different,  though  allied,  agricultural  capabilities.  The  oak  open- 
ings are  most  nearly  related  to  the  prairies,  while  the  oak  forests 
graduate  towards  the  following  classes.  Those  plants  which  have  been 
mentioned  as  preferring  association  with  the  subsequent  groups,  as  the 
Pignut  Hickory,  Great-toothed  Poplar,  etc.,  are  found  chiefly  in  the 
forests,  and  much  more  rarely  in  the  openings,  while  of  the  species 
common  to  the  prairie  and  oak  groups,  the  majority  are  only  found 
in  the  openings,  and  but  few  in  the  denser  oak  forests. 

CLASS  III.  The  Oak  and  Maple  Group.  It  is  difficult  to  draw 
sharp  lines  of  demarkation  between  the  several  classes  of  heavy  forests, 
and  to  circumscribe  the  areas  occupied  by  each.  The  fact  is,  that  no 
abrupt  line  of  separation  exists.  But  perhaps  the  distinctions  here 
attempted  are  as  clear  and  as  legitimate  as  in  many  other  departments 
of  science,  where  such  distinctions  are  sanctioned,  and  for  the  practi- 
cal ends  for  wThich  this  investigation  is  made,  it  is  essential  that  such 
divisions  should  be  attempted,  and  besides  the  tout  ensemble  is  dis- 
tinct, though  the  constituents  may  be  linked  into  the  groups  on  either 
hand.  These  observations  seem  especially  demanded  as  an  introduc- 
tion to  the  definition  of  this  class.  The  oaks  which  have  been  made 
the  most  conspicuous  characteristic  of  the  preceding  group  are  made 


NATIVE  VEGETATION.  179 

joint  partners  in  naming  this  division,  and  will  be  found  to  mingle 
with  those  that  follow.  The  maples  which  are  here  introduced  to 
our  attention  will  also  play  a  conspicuous  part  in  subsequent  classifi- 
cations. This  group  is  not  then  characterized  by  the  exclusive  pres- 
ence of  any  prominent  plant,  but  by  a  distinctive  association  of  plants 
common  to  several  classes. 

The  White  Oak  is  the  most  prominent  of  its  genus,  and  attains  a 
large  size.  The  Red  Oak  and  Burr  Oak  are  usually  present.  Their 
proportionate  number  is  very  much  the  same  as  in  the  denser  oak 
groves  of  the  preceding  group.  But  to  these  oaks  there  is  added  the 
Hard  or  Sugar  Maple  (Acer  saccharinum),  and  the  Red  Maple  (Acer 
rubrum).  The  latter  seerns  to  have  its  best  development  in  this  asso- 
ciation. The  Elms  ( Ulmus  Americana  and  V.  ful'oa)  are  more  or 
less  present,  but  not  prominent,  as  also  the  Linden  or  Basswood  (Tilia 
Americana).  The  Iron  wood  (Ostrya  Virginica),  and  the  Beech 
(Fagus  ferruginea)  are  excluded  from  this  group.  The  White  Ash 
(Fraxinus  Americana)  is  rarely  seen  in  this  connection,  but  the 
Black  Ash  (Fraxinus  sambucifolia)  is  common  in  contiguous  low- 
lands. The  Hazel  (Corylus  Americana}  is  not  prominent  though 
present,  and  the  Cornus paniculata  of  the  last  group  is  largely  replaced 
by  Cornus  circinata. 

CLASS  IY.  Maple  Group.  The  leading  member  of  this  group  is 
the  Sugar  Maple  (Acer  saccharinum);  not  that  at  every  point  it  is 
more  numerous  than  any  and  all  others,  but  that  on  the  average  it 
surpasses  the  other  species.  This  is,  however,  in  a  high  sense,  a 
mixed  group,  and  embraces  some  of  the  densest  forests  of  the  state. 
The  Oaks  of  the  last  group  are  present  here  also,  but  ift  less  numbers 
and  in  subordination  to  other  species.  The  Linden  (Tilia  Ameri- 
cana) is  very  numerous.  The  White  Elm  (  Ulmus  Americana)  which 
in  the  areas  occupied  by  the  foregoing  classes  was  chiefly  confined  to 
the  low  lands  and  river  bottoms,  here  extends  itself  more  upon  the 
highlands,  and  is  intimately  intermingled  with  a  large  assemblage  of 
species.  The  Ulmus  fulva  is  also  present.  Both  the  White  and 
Black  Ash  are  found,  the  latter  in  the  lower  lands.  The  Ironwood 
(Ostrya  Virginica)  is  abundant  and  highly  characteristic.  The  Black 
Walnut  (Juglans  nigra),  and  the  Butternut,  (Juglans  cinerea)  are  com- 
mon. The  Carya  alba  (Hickory)  is  chiefly  replaced  by  Carya  gldbra 
(Pignut),  and  similarly  the  Populus  tremuloides  gives  place  to  the 
Populus  grandidentata.  The  White  Thorn  (Cratwgus  coccinea)  is 
common,  while  the  Crab  Apple  (Pyrus  coronaria)  is  correspond- 
ingly rare.  The  Wild  Plum  (Prunus  Americana)  is  less  abundant 
than  in  the  Oak  group,  while  its  congener,  the  Black  Cherry  (Pru- 


180  GEOLOGY  OF  EASTERN  WISCONSIN. 

nus  serotina)  grows  to  ampler  proportions.  The  Paper  or  Canoe 
Birch  (Betula  papyracea)  is  occasionally  found  in  favorable  local- 
ities, but  is  not  strictly  a  member  of  the  class.  The  Beech  (Fagus 
ferruginea)  is  excluded  and  made  characteristic  of  the  following 
group. 

Of  shrubs,  the  Round-leaved  Cornel  (Cornus  circinata)  exceeds  all 
others,  and  almost  entirely  excludes  the  Hazel  and  Panicled  Cornel, 
the  dominant  forms  in  the  Oak  group. 

The  herbaceous  vegetation  is  similarly  well  characterized,  but  for 
the  reasons  previously  assigned,  will  not  be  dwelt  upon  here.  This  is 
a  well  marked  group,  and  its  distribution  is  highly  significant. 

CLASS  Y.  Maple  and  Beech  Group.  This  group  is  essentially 
the  same  as  the  preceding,  with  the  addition  of  the  Beech  (Fagus 
ferruginea).  This  separate  class  for  a  single  tree  and  a  few  subordi- 
nate associates  is  thought  to  be  justified  by  the  fact  that  the  Beech  is 
confined  to  the  lake  region,1  and  appears  to  be  especially  indicative  of 
lake  influence,  as  it  occupies  different  classes  of  soils  and  covers  dif- 
ferent geological  formations.  There  is  less  oak  in  this  than  in  the 
preceding  class. 

CLASS  YI.  The  Hardwood  and  Conifer  Group.  This  class  con- 
sists of  a  modification  of  the  last,  and  the  important  addition  of  the 
Conifers.  One  of  the  more  conspicuous  modifications  is  the  more  or 
less  complete  disappearance  of  those  representatives  of  the  Oak  group 
that  have  lingered  through  the  foregoing  classes.  The  Ironwood  is 
far  less  abundant;  the  Black  Walnut  and  Butternut  are  rare;  the 
Witch  Hazel  (Hamarnelis  Virginica),  and  the  Mountain  Maple 
(Acer  spicatum)  appear  more  prominently  among  the  underbrush. 
The  berry-bearing  plants  are  multiplied,  as  if  to  compensate  for  the 
disappearance  of  the  larger  fruit-bearers.  These  changes  are  pro- 
gressive as  we  penetrate  the  area  occupied  by  this  class. 

Of  the  Conifers,  the  first  to  be  introduced  is  the  White  Pine  (Pi- 
nits  strobus),  if  we  except  the  Arbor  Yitae  (Thuja  occidentalis),  which 
from  its  proneness  to  swampy  land  and  other  selected  localities  can 
scarcely  be  considered  a  member  of  this,  as  an  upland  group.  Far- 
ther to  the  north,  the  Red  Pine,  commonly  called  Norway  Pine  (Pi- 
nus  resinosa),  becomes  somewhat  common.  The  Hemlock  (Abies 
Canadensis)  is  one  of  the  most  prominent  and  abundant  members  of 
the  group.  The  Balsam  Fir  (Abies  balsamea),  although  preferring 
the  immediate  vicinity  of  water,  mingles  somewhat  with  the  group, 
especially  in  its  northern  extension.  It  is  especially  abundant  on  the 
shores  of  the  Green  Bay  peninsula.  An  occasional  Spruce  (Abies 

'See  article  of  I.  A.  Lapham,  Trans.  Wis.  State  Agri.  Soc.,  1854-5-6-7,  p.  236. 


NATIVE  VEGETATION.  181 

nigra)  wanders  away  from  its  marshy  habitat,  and  the  Arbor  Vitae 
extends  itself  quite  freely  upon  the  uplands. 

CLASS  VII.  Pine  Group.  This  includes  the  well  known  vegeta- 
tion of  the  "Pine  Lands."  It  is  here  made  to  include  those  regions 
over  which  the  pine  is  predominant  in  distinction  from  those  in 
which  it  is  simply  scattered  through  prevailing  hardwood  timber,  as 
in  the  preceding  group.  The  leading  tree  is  the  Pinus  strobus. 

CLASS  VIII.  Limestone  Ledge  Group.  This  is  a  small  but  inter- 
esting vegetal  cluster,  covering  limited  areas  in  which  there  is  the 
most  meager  soil,  resting  upon  limestone.  In  this  heavy  drift  region, 
such  areas  are  few  and  small,  but  the  distinctness  of  the  flora  is  so 
marked,  and  so  well  illustrates  the  fundamental  principle  upon  which 
the  value  of  all  these  observations  rests,  that  it  merits  a  name  and 
place  as  a  separate  class.  The  Poplars  (Populus  tremuloides,  grandi- 
dentata,  and  balsamifera),  the  Canoe  Birch  (Betula  papyracea),  the 
Snowberry  (Symphoricarpus  racemosus],  the  Smooth  Sumac  (Rhus 
glabrd],  with  the  Conifers,  constitute  the  major  vegetation,  and  rather 
from  the  combination  than  from  the  constituents,  cause  it  to  stand 
out  in.  marked  contrast  to  the  heavy  timber  by  which  it  is  fre- 
quently encompassed.  It  forms  a  thicket  rather  than  a  forest. 
The  most  characteristic  feature  is  the  abundance  of  the  Poplars  and 
the  Birch. 

The  Populus  tremuloides  is  not  common  in  the  forests  by  which 
the  typical  areas  of  this  class  are  surrounded,  which  makes  its  abund- 
ance here  the  more  conspicuous. 

The  Rubus  strigosus,  Cornus  circinata  and  Lonicera  parviflora 
are  attendant  shrubby  plants.  The  herbaceous  vegetation  is  also 
peculiar. 

CLASS  IX.  The  Comprehensive  Group.  This  class  consists  of  a 
commingling  of  nearly  all  the  arboreal  species  of  the  foregoing  groups. 
Clusters  may  be  selected  that  are  representatives  of  nearly  all  the 
other  classes,  but  in  general  the  species  are  curiously  mingled,  and  do 
not  array  themselves  in  the  definite  associations  that  characterize  the 
preceding  groups.  It  is  most  nearly  allied  to  the  Maple,  Beech  and 
Conifer  group,  and  lies  contiguous  to  it,  and  near  the  limit  of  marked 
lake  influence. 

B.    MARSH  VEGETATION. 

CLASS  X.  The  Grass  and  Sedge  Group.  This  includes  the  well 
known  occupants  of  our  open  meadow  .marshes.  It  corresponds  to 
the  prairie  group  among  upland  vegetation,  and  in  many  cases  gradu- 
ates imperceptibly  into  it.  It  embraces  several  subordinate  groups 


182  GEOLOGY  OF  EASTERN  WISCONSIN. 

which  are  very  indicative  of  the  nature  of  the  marsh  bottom  on 
which  they  grow,  but  which  can  scarcely  be  described  in  a  manner 
intelligible  to  the  general  reader,  although  they  are  readily  distin- 
guished by  observing  farmers.  It  may  be  remarked  in  general,  how- 
ever, that  the  better  class  consist  of  the  grasses  proper  (Graminece), 
not  only  because  they  are  in  themselves  valuable,  but  also  because 
they  indicate  a  bottom  susceptible  of  easy  improvement  by  the  sub- 
stitution of  more  valuable  grasses.  The  Sedges  (Cyperaceos)  in  gen- 
eral occupy  marshes  that  are  of  inferior  value  now,  and  are  less 
promising  of  immediate  returns  to  labor  spent  in  improvement. 
Fortunately  the  former  class  largely  predominate. 

CLASS  XI.  The  Heath  Group.  This  association  of  swamp  vege- 
tation is  characterized  by  the  predominance  of  the  members  of  the 
Heath  family  (Ericaceae).  Among  these  the  most  characteristic 
plant  is  the  Leather  Leaf  (Cassandra  calyculata),  and  the  most  im- 
portant one  is  the  Cranberry  (  Vaccinium  macrocarpon).  The  "Wil- 
low, Larch  and  Sphagnum  mosses  and  a  variety  of  other  plant's  are 
very  frequent  associates.  This  class  is  worthy  of  attention,  not  so 
much  in  view  of  its  prominence  as  a  botanical  group,  as  on  account 
of  its  present  and  prospective  economic  importance.  The  actual  ex- 
istence of  the  cranberry  plant  in  its  native  state  assures  us  of  condi- 
tions favorable  to  its  growth  and  indicates  where  cultivation  will  be 
most  likely  to  prove  remunerative.  Where  the  cranberry  itself  is 
not  present,  it  is  eminently  desirable  to  know  what  plants  are  its  ha- 
bitual associates  and  demand  similar  conditions  of  soil  and  moisture, 
since  these  may  be  almost  equally  good  guides  in  the  selection  of  a 
suitable  marsh  for  improvement.  Of  plants  which  serve  this  purpose 
the  Cassandra  calyculata  is  regarded  as  the  most  reliable.  On  this 
point  an  excellent  work  on  the  subject  says:  "  In  selecting  a  loca- 
tion it  is  very  important  to  observe  the  varieties  of  plants  or  trees 
existing  upon  the  ground.  Although  no  cranberry  vines  may  be 
growing  there,  yet  the  presence  of  other  plants  requiring  similar 
conditions  of  soil  and  moisture  indicate  a  soil  congenial  cothe  growth 
of  the  cranberry.  For  instance,  the  Feather-leaf,  also  called  Gander- 
bush  and  Leather-leaf  (Cassandra  calyculata\  so  abundant  in  heath 
ponds,  is  considered  a  sure  indication  of  a  proper  locality." 

The  distribution  and  additional  facts  relative  to  this  group  will  be 
given  a  few  pages  in  advance. 

CLASS  XII.  The  Tamarac  Group.  The  name  is  perhaps  a  suffi- 
cient definition  even  to  the  commonest  observer.  The  Tarnarac  or 
American  Larch  (Larix  Americana}  constitutes  the  entire  arboreal 

1  Cranberry  Culture,  by  J.  J.  White. 


NATIVE  VEGETATION.  183 

growth;  the  Ericacece  form  the  chief  undergrowth,  and  the  Sphag- 
noid  mosses  carpet  the  peaty  bottom,  forming  a  well-marked  flora. 

CLASS  XIII.  The  Arbor  Vitce  Group.  This  is  similar  to  the  last 
save  that  the  Arbor  Yitse,  or  White  Cedar,  as  it  is  frequently  called 
(Thuja  occidentalis\  takes  the  place  in  whole  or  in  part  of  the  Tama- 
rac.  Usually  the  Tamarac  is  present  in  greater  or  less  numbers.  A 
not  unfrequent  arrangement  consists  of  a  predominance  of  the  Arbor 
Yitse  around  the  borders  of  the  swamp,  and  of  the  Tamarac  toward  the 
center.  The  latter  is  a  more  thoroughly  swamp  species  (although  oc- 
casionally seen  on  the  hillsides)  than  the  former. 

CLASS  XIY.  The  Spruce  Group.  This  is  similar  to  the  two  pre- 
ceding groups,  except  that  the  Black  Spruce  (Abies  nigra)  is  the  chief 
arboreal  form.  The  Larch  and  Arbor  Yitee  are  frequently  present.  As 
the  Spruce  is  confined  to  the  northern  regions,  more  of  the  northern 
forms  of  minor  vegetation  are  associated  with  this  group,  although 
the  same  tendency  is  shown  in  the  other  classes  in  the  same  latitude. 

From  the  habit  of  these  three  paludal  conifers  of  mingling,  it  is 
sometimes  difficult  to  classify  a  given  swamp,  and  it  has  not  been 
thought  important  to  distinguish  them  on  the  accompanying  map  of 
vegetation,  although  they  were  so  distinguished  on  the  original  map. 


C.    GROUPS  INTERMEDIATE  BETWEEN  THE  UPLAND  AND  MARSH 

GROUPS. 

CLASS  XY.  The  Slack  Ash  Group.  In  this,  as  the  name  implies, 
the  Black  Ash  (Fraxinus  sambucifolia]  is  the  predominating  plant. 

The  Black  Alder  (Alnus  incana)  is  a  subordinate  and  quite  constant 
associate,  and  the  two  characterize  the  group.  The  Arbor  Yitse  is  fre- 
quently present,  and  sometimes  the  Witch  Hazel.  Otherwise,  as  far  as 
observed,  the  association  is  not  constant. 

CLASS  XYI.  The  Yellow  JSirch  Group.  This  is  not  altogether  a 
well  defined  group.  The  abundance  of  Yellow  Birch  (Betula  lutea, 
excelsa)  is  the  most  marked  feature  of  the  vegetation.  The  Hemlock 
is  very  common,  and  the  Maples  and  Beech  are  present.  Under  the 
dense  shadow  of  these,  several  species  of  Lycopodium,  the  Dwarf 
Yew  (Taxus  Canadensis],  the  large  Purple-flowered  Easpberry  (Rubus 
odoratus\  the  Ericaceae  (Pyrola  rotundifolia  and  secunda\  the  Co- 
hosh  (Actea  spicata,  var.  alba)  abound  among  others,  though  the 
most  of  these  are  present  in  other  groups.  This  group  occupies  only 
some  limited  areas  in  the  peninsula  east  of  Green  Bay,  and  in  the 
press  of  other  duties,  sufficient  opportunity  was  not  afforded  for  satis- 
factory study. 


184  GEOLOGY  OF  EASTERN  WISCONSIN". 

Distribution.  On  the  accompanying  map  of  vegetation,  the  dis- 
trict covered  by  each  of  these  classes  is  delineated,  with  as  much  of 
detail  and  accuracy  as  was  compatible  with  the  demand  of  other  de- 
partments of  the  survey,  and  with  the  rapidity  necessitated  by  the 
large  area  examined.  As  that  presents  their  distribution  far  more 
vividly  and  accurately  than  any  verbal  description,  I  need  only  add 
here  a  few  supplementary  remarks. 

It  will  be  seen  by  consulting  the  map,  that  the  prairies  are  almost 
exclusively  confined  to  the  southwestern  portion  of  the  district,  or 
chiefly  to  the  Mississippi  drainage  system,  though  this  fact  perhaps 
has  no  special  significance.  The  surface  of  a  portion  of  these  prairies 
is  level,  and  bears  evidence  of  having  formerly  been  a  lake  bottom, 
while  that  of  others  is  elevated  and  undulating,  and  bears  no  evidence 
of  having  been  submerged  since  the  retreat  of  the  glacier.  The  areas 
of  prairie  and  forest  are  so  intermingled  as  to  forbid  any  topogra- 
phical distinction  between  them,  and  to  negative  any  explanation  of 
their  origin  that  is  dependent  on  surface  features.  It  is  not  proposed 
to  enter  here  upon  the  much  discussed  question  of  the  origin  of  prai- 
ries, but  simply  to  remark  that  the  tenor  of  the  facts  in  this  region, 
bearing  upon  the  question,  supports  the  general  views  so  ably  pres- 
ented by  Profs.  Dana,  dewberry,  Guyot  and  others,  and  at  the  same 
time  harmonizes  with  the  observations  of  Prof.  Whitney,  to  the  ex- 
tent that  the  nature  of  the  soil  is  the  most  essential  primary  agency. 
It  is  not  however  because  the  soil  is  incapable  of  supporting  trees,  for 
when  planted  upon  the  prairies  they  flourish  luxuriantly,  and  when 
the  soil  is  cultivated  or  shaded  so  that  a  proper  degree  and  constant 
supply  of  moisture  is  secured,  trees  are  propagated  from  the  seed  with 
facility.  In  the  first  case,  in  planting  the  trees,  the  superficial  com- 
pact soil,  which  is  believed  to  be  the  real  barrier  to  the  extension  of 
the  forests  in  itds  region,  is  penetrated,  and  the  roots  of  the  tree 
placed  below  it,  and  it  is  at  the  same  time  loosened,  and  mingled  with 
the  subsoil;  and  in  the  second  case,  artificial  stirring  of  the  soil  or 
special  conditions  supply  the  moisture  essential  to  the  growth  of  ar- 
boreous vegetation.  But  in  its  native,  undisturbed  condition,  the  fine 
superficial  soil  becomes  exceedingly  dry  at  intervals  during  the  sea- 
son, and  renders  it  impossible  or  exceedingly  difficult  for  the  young 
seedling  to  maintain  its  existence  until  it  can  gain  a  foot-hold  upon 
the  deeper  and  uniformly  moist  subsoil.  This  difficulty  is  increased 
by  the  antagonism  of  the  grasses  that  can  successfully  withstand  these 
variations  of  moisture,  and  by  annual  fires.  The  latter  have  doubt- 
less modified  the  form  and  extent  of  the  prairies  in  some  degree,  but 
it  is  generally  conceded  by  those  who  have  studied  the  subject  com- 


NATIVE  VEGETATION.  185 

preliensively,  that  it  is  entirely  inadequate  as  an  explanation  of  prai- 
ries in  general. 

The  Oak  group  is  likewise  chiefly  confined  to  the  southwestern  part 
of  the  district.  It  occupies  all  classes  of  topography  and  all  eleva- 
tions from  the  lake  level  to  500  feet  above  it.  It  shows  a  tendency  to 
invade  the  districts  of  the  heavier  forests,  along  the  line  of  the  Kettle 
Range.  This  is  due  to  the  nature  of  the  soil  that  accompanies  the 
Range,  as  will  be  seen  hereafter. 

The  Oak  and  Maple  group  usually  lies  contiguous  to  the  last  or 
along  the  Kettle  Range.  It  was  in  the  latter  relationship  that  its  pe- 
culiarities were  first  and  chiefly  noticed.  This  seems  to  be  due  to  the 
fact  that  the  soil  is  adapted  to  the  Oak  group,  while  the  surroundings 
are  favorable  to  the  propagation  of  the  Maple  and  its  associates.  A 
conflict  of  conditions  is  the  result,  in  which  neither  has  a  decided  ad- 
vantage. 

The  Maple  group  occupies  an  irregular  belt  that  has  a  northwest 
and  southeast  trend,  bordered  chiefly  by  Oaks  on  the  south  and  Beech 
and  its  associates  on  the  north.  It  is  quite  distinctly  limited  in  the 
direction  of  the  Oaks,  but  much  less  so  toward  the  Oak  and  Maple,  and 
the  Maple  and  Beech  groups,  into  which  it  merges  almost  impercepti- 
bly. It  reaches  from  the  lake  shore  to  about  500  feet  in  elevation. 

The  Maple  and  Beech  group  covers  a  large  surface  stretching  from 
the  lake  shore  northwestward,  a  direction  which  neither  corresponds 
to  geological  nor  topographical  lines,  but  is  none  the  less  instructive 
on  that  account.  It  does,  however,  correspond  very  closely  with  the 
isothermals  for  the  summer  months; l  which,  with  the  other  elements 
of  the  lake  influence,  as  already  intimated,  are  undoubtedly  the  con- 
trolling agencies. 

To  the  north  of  this  the  Hardwood  and  Conifer  group  extends  to  Port 
de  Morts,  being  more  extensive  than  either  of  the  others.  The  great- 
est elevation  within  its  area  is  less  than  400  feet  above  Lake  Michigan. 

The  Comprehensive  group  occupies  a  portion  of  the  crest  and  west- 
ern slope  of  the  outcropping  rocky  ridge  of  our  district.  It  is  limit- 
ed chiefly  to  the  Green  Bay  region.  It  seems  to  be  the  result  of  the 
conflicting  demands  of  lake  and  boreal  influences,  on  the  one  hand, 
and  of  soil  and  warm,  dry  southwest  winds,  sweeping  up  the  Green 
Bay  valley,  on  the  other. 

1  See  Map  of  Wisconsin  with  lines  showing  the  Remarkable  Effect  of  Lake  Michigan 
in  Elevating  the  Temperature  for  January  and  Depressing  that  of  July,  by  I.  A.  Lap- 
harn,  1865.  Also  Transactions  Chicago  Academy  of  Sciences,  Vol.  I,  Plate  X,  1865.  See 
also,  The  Isothermal  Lines  of  Wisconsin,  by  J.  G.  Knapp,  Transactions  Wisconsin  Hor- 
ticultural Society,  Madison,  1871. 


186  GEOLOGY  OF  EASTERN  WISCONSIN. 

In  the  lowlands,  the  Grass  and  Sedge  marshes  which  correspond  to, 
and  in  many  cases  are,  unquestionably  the  forerunners  of  the  prairies, 
are  like  them,  chiefly  confined  to  the  southwestern  region. 

As  we  enter  the  dense  forests  to  the  north,  the  Tamarac  swamps 
almost  entirely  replace  them,  and  these  in  turn,  in  the  still  higher 
latitudes,  are  in  part  replaced  by  the  Cedar  and  Spruce  swamps.  The 
Ash  swamps  are  more  abundant  and  extensive  at  the  north,  and  the 
Yellow  Birch  flats  are  entirely  northern. 

The  distribution  of  the  Heath,  or  Cranberry  group,  is  not  less  in- 
teresting than  important.  The  marshes  occupied  by  this  class  readily 
arrange  themselves,  on  inspection,  into  four  clusters,  having  a  definite 
relationship  to  the  geological  formations.  Those  in  the  northwestern 
part  of  the  district  are  to  be  grouped  with  the  great  marshes  near 
Berlin  and  to  the  -.vestward,  and  rest  upon  the  Potsdam  sandstone. 
Those  in  the  western  part  of  Jefferson  county  lie  upon,  or  near,  the 
St.  Peters  sandstone.  Those  in  Oconomowoc,  Concord,  Hebron,  Sum- 
mit, Delafield,  Ottawa,  Eagle,  Richmond  and  Sugar  Creek,  form  a 
numerous  group  of  small  marshes,  and  rest  upon  a  sandy  district  that 
seems  to  have  had  its  origin  in  drift  from  the  arenaceous  layers  of  the 
Cincinnati  shale,  subsequently  modified  by  lake  action,  of  which  the 
swamps  are  the  lingering  representatives.  The  fourth  group  com- 
prises those  that  lie  along  the  line  of  the  ancient  sand  beaches  of  Lake 
Michigan,  of  which  the  marshes  near  Sturgeon  Bay  and  Peshtigo  are 
examples.  The  demand  for  silica  is  thus  shown  in  the  natural  dis- 
tribution of  the  plant,  and  we  have  in  this  a  beautiful  illustration  of 
the  fundamental  principle  insisted  upon  in  this  report.  Native  cran- 
berries occur  at  the  following  locations: 

Sugar  Creek,  T.  3,  R.  16  E.    Sec.  18. 

Richmond,  T.  3,  R.  15  E.    Sec.  18. 

Eagle,  T.  5,  R.  17  E.    Sec.  31,  N.  W.  qr. 

Ottawa,  T.  6,  R.  17  E.    Sees.  32  and  28. 

Hebron,  T.  6,  R.  15  E. 

Lake  Mills,  T.  7,  R.  13  E. 

Concord,  T.  7,  R.  16  E.    Sec.  26. 

Summit,  T.  7,  R,  17  E.    Sees.  9  and  12,  N.  W.  qr. 

Delafield,  T.  7,  R.  18  E.    Sec.  34,  N.  E.  qr.,  and  sec.  27,  S.  E.  qr. 

Oconomowoc,  T.  8,  R.  17  E.    Sec.  4. 

Oakland,  T.  6,  R.  13  E.    Sec.  3,  S.  W.  qr.,  and  sec.  17. 

Sturgeon  Bay,  T.  27,  R.  26  E.    Sec.  12,  W.  Lf. 

Caledonia,  T.  21,  R.  14  E.    Sec.  29. 

Peshtigo  and  Marinette,  T.  30,  R,  23  E.     Sec.  21  and  adjoining. 

Aurora,  T.  18,  R.  13  W.,  where  the  marshes  occupy  several  sections  east  and 

southeast  of  the  village  of  Auroraville,  and  are  among  the  most  extensive  and 

productive  in  the  state. 


NATIVE  VEGETATION.  187 

Doubtless  they  occur  also  at  other  points  that  escaped  my  knowl- 
edge. AYhen  it  is  considered  that  the  size  of  the  district  required 
the  inspection  of  from  3,000  to  4,000  square  miles  each  season,  some 
omissions  in  matters  not  specifically  geological  will  doubtless  be  par- 
doned by  a  generous  public. 

The  elements  of  success  in  cranberry  culture,  so  far  as  they  are  rel- 
evant here,  seem  to  be  the  following,  as  I  glean  from  several  author- 
ities: 

I.  A  Suitable  Bottom.     A  good  bed  of  peat  is  the  best,  that  being 
the  principal  food  of  the  plant.     At  the  east,  cedar  swamp  bottoms 
are  preferred   by  many.     Our   tamarac   swamps   will  doubtless   be 
equally  satisfactory;  indeed,  native  cranberries  are  sometimes  found 
growing  on  them. 

II.  Facilities  for  drainage,  and  complete  control  of  it,  so  that  the 
marsh  may  be  drained  or  flooded,  as  may  be  demanded. 

III.  A  Sufficient  Supply  of  Silica.     This  is  sometimes  already 
present,  but  is  usually  to  be  supplied  by  covering  the  surface  with 
sand.     "Silica  plants"  differ  from  "peat  plants"  in  appearance  and 
mode  of  growth,  and  in  yielding  at  least  three  times  the  amount  of 
fruit  produced  by  the  latter.     The  successful  culture  of  the  cranberry 
is  also  limited  to  certain  latitudes.     If  too  far  north,  the  early  frosts 
prevent  their  maturing  and  render  them  a  precarious  crop.     If  too  far 
south,  the  heat  interferes  with  their  proper  development.     Actual  ex- 
perience is  the  best  guide  in  respect  to  this,  as  well  as  the  other  con- 
ditions, and  hence  the  value  of  observations  on  the  experiments  that 
Mature  has  herself  made. 


188  GEOLOGY  OF  EASTERN  WISCONSIN. 


CHAPTER  IV. 
SOILS. 

There  are  few  subjects  upon  which  it  is  more  difficult  to  make  an 
accurate,  aud  at  the  same  time  an  intelligible  report,  than  upon  soils. 
This  difficulty  arises  partly  from  the  nature  of  the  subject,  and  partly 
from  the  vagueness  of  the  terms  used  in  speaking  of  soils.  Aside 
from  the  vagueness,  these  terms  have  a  different  signification  as  used 
by  different  persons,  which  adds  to  the  difficulty.  We  speak  of  "  light 
soils  "  and  "  heavy  soils,"  and  perhaps,  without  thinking,  we  suppose 
that  these  terms  refer  to  actual  weight,  or,  in  the  terms  of  science, 
to  specific  gravity.  But  such  is  not  usually  the  fact.  Thus,  we  say, 
"a  heavy  clay  soil"  and  "a  light  sandy  soil,"  but  in  fact  the  weight 
of  the  clay  soil  is  only  about  three-quarters  of  that  of  the  sandy  soil, 
measure  for  measure.  These  terms,  as  commonly  used,  really  refer 
to  adhesiveness,  degree  of  comminution,  or  power  of  holding  water, 
or,  more  properly,  perhaps,  to  the  way  in  which  the  soil  "works." 
Again,  the  term  "  sandy  soils  "  is  supposed,  even  by  persons  some- 
what versed  in  the  sciences,  to  mean  those  that  are  made  up  of  grains 
of  quartz;  or,  in  other  words,  are  silicious,  and  hence  are  more  or  less 
barren.  But  this  is  not  always  true.  Some  sandy  soils  are  composed 
of  grains  of  limestone,  and  are  very  fertile,  an  instance  of  which  will 
be  described  presently.  So,  a  clay  soil  is  supposed  by  many  some- 
what intelligent  in  chemistry,  to  be  composed  of  aluminous  material, 
but  this  is  far  from  always  being  the  case,  as  the  term  is  commonly 
used. 

This  obscurity  will,  however,  in  a  measure,  disappear  as  we  proceed 
to  consider  the  origin  of  the  soils  of  Eastern  Wisconsin,  which  appro- 
priately claims  our  attention  here. 

The  organic  constituents  of  the  soil  have  manifestly  been  derived 
from  the  plants  that  the  soil  has  itself  produced,  and  are  only  the  re- 
sult of  accumulated  self -enrichment.  Local  exceptions  to  this  are  to 
be  found  in  those  cases  where  soils  have  received  organic  material 
washed  from  adjacent  areas.  This  vegetable  matter  takes  various 
forms,  but  all  may  be  spoken  of  under  the  comprehensive  term, 
liumus.  In  marshy  locations,  the  moisture  prevents  the  decay  of 


SOILS. 

vegetable  accumulations  to  such  an  extent  that  the  resulting  humus 
forms  the  main  constituent  of  the  soil,  and  the  mineral  ingredients 
are  entirely  subordinate  in  amount  and  function,  thus  forming  a  soil 
of  vegetable  origin. 

"With  this  exception,  the  leading  elements  of  our  soils  are  derived 
directly  or  indirectly  from  the  rocks,  either  through  their  powdering 
by  mechanical  means,  or  disintegration  by  chemical  agencies.  The 
chief  mechanical  agent  in  pulverizing  the  rocks  has  been  water  in  its 
various  states,  especially  in  the  form  of  glacial  ice.  When  the  great 
glacier  plowed  over  this  region,  it  broke  fragments  from  every  forma- 
tion over  which  it  passed,  ground  them  to  various  stages  of  commin- 
ution, and  left  the  commingled  mass  spread  over  the  face  of  the  coun- 
try, forming  a  most  excellent  foundation  for  our  soils.  Subsequently, 
water  in  the  form  of  lakes  and  rivers  washed  out  and  redeposited  a 
portion  of  this  material,  giving  rise  to  sandy  beach  lines  and  lacus- 
trine and  fluviatile  deposits  of  clay. 

But  this  material  was  still  too  crude  to  constitute  a  fertile  soil,  and 
besides,  over  many  small  areas,  these  agencies  left  the  rock  entirely 
bare.  Then  followed  a  process  of  disintegration,  of  a  chemical  or 
chemico-physical  nature,  popularly  spoken  of  as  the  action  of  the  ele- 
ments, by  which  the  surface  of  this  material,  and  the  rock  surface, 
where  exposed,  was  reduced  to  the  condition  of  soil,  which  in  the  pro- 
gress of  ages  enriched  itself  by  its  own  vegetation.  It  appears,  then, 
that  (1)  a  portion  of  our  soils  were  derived  directly  from  the  glacial 
accumulations,  and  are  properly  called  drift  soils;  that  (2)  a  portion 
were  derived  from  the  same  kind  of  material,  but  after  it  had  been 
washed  and  redeposited  by  lake  and  river  action,  forming  soils  of 
lacustrine  and  fluviatile  origin;  and  (3)  that  another  portion  had  their 
origin  in  the  direct  decomposition  of  the  undisturbed  rock  formations. 
It  will  now  be  clear  that  the  character  of  a  soil  will  depend  upon  (1) 
the  nature  of  the  rock  from  which  it  was  derived;  (2)  the  manner  and 
degree  of  its  reduction ;  (3)  the  amount  lost  by  leaching  and  other- 
wise; and  (4)  the  amount  gained  by  vegetation  from  above  or  capil- 
lary action  from  beneath.  Or,  to  put  the  matter  much  more  simply, 
a  soil  depends  chiefly  upon  (1)  the  chemical  nature  of  the  material, 
and  (2)  its  physical  state  or  the  degree  of  fineness  to  which  it  is  re- 
duced. These  elements  will  receive  prominent  attention  in  the  de- 
scriptions of  soil  that  follow. 

To  fully  understand  the  nature  of  the  material,  all  the  rock  forma- 
tions of  the  region  and  those  that  lie  to  the  north  and  east,  whence 
the  glacier  came,  should  be  studied,  since  they  have  all  made  contri- 
butions to  our  highly  composite  soils,  and  herein  the  strictly  geologi- 


190  GEOLOGY  OF  EASTERN  WISCONSIN. 

cal  relations  of  the  subject  are  apparent.  It  will  be  sufficient  here, 
however,  to  call  attention  to  the  four  general  classes  of  rocks  that 
have  chiefly  entered  into  the  formation  of  the  soils  of  the  part  of  the 
state  under  consideration,  and  for  fuller  knowledge,  refer  the  reader 
to  the  general  report.  These  are  (1)  the  Archaean  rocks,  whose  min- 
eral nature  is  very  complex,  but  which  give  rise  chiefly  to  silicious 
and  aluminous  material;  (2)  the  sandstones  that  contribute  silica;  (3) 
the  shales,  that  are  chiefly  aluminous;  and  (4),  most  abundant  and 
important  of  all,  the  dolomites  or  magnesia,n  limestones,  that  contrib- 
ute lime  and  magnesia.  Soda,  potash,  phosphorus,  and  other  ingre- 
dients, exist  in  small  quantities  in  the  several  formations.  The  lime 
and  magnesia  occur  chiefly  in  the  form  of  carbonates,  and  their  pres- 
ence is  manifested  by  effervescence  on  the  application  of  acid,  with 
which  the  soils  were  extensively  tested  in  the  field. 

The  following  descriptions  of  the  soils  of  the  district  under  con- 
sideration relate  rather  to  the  subsoil  than  the  soil  proper;  at  least 
there  has  been  an  effort  to  set  aside  purely  surface  characters,  first, 
because  the  surface  soil  is  subject  to  so  many  local  and  changeable 
influences,  and  has  been  so  much  modified  by  cultivation  and  other 
artificial  causes,  that  a  series  of  observations  upon  typical  or  "virgin  " 
soils  was  scarcely  possible,  and  secondly,  because  the  future  of  our 
agriculture  depends  not  so  much  upon  the  present  soil  as  upon  the 
subsoil,  since  winds,  waters  and  cropping  are  rapidly  sweeping  the 
surface  away,  and  but  comparatively  few  years  will  pass  before  our 
present  subsoil  will  be  at  the  surface,  and  for  the  further  reason  that 
the  power  of  the  surface  soil  to  retain  the  strength  it  has,  and  to  draw 
mineral  resources  from  below,  is  most  evidently  dependent  on  the 
subsoil. 

If,  in  reading  the  descriptions  that  follow,  the  reader  will  be  kind 
enough  to  place  before  him  Plate  III  of  the  accompanying  atlas,  the 
areas  occupied  by  each  class  will  be  seen  more  definitely  than  they 
could  be  presented  by  description,  which  will  then  be  for  the  greater 
part  omitted.  It  will  be  readily  understood  by  every  one,  that  soils 
vary  much  in  every  section,  and  even  on  the,  same  farm,  and  that  the 
varieties  graduate  into  each  other  in  the  most  intricate  and  impercep- 
tible manner,  and  yet  at  the  same  time  every  region  has  a  prevailing 
character  that  can  be  classed,  described  and  mapped.  The  accom- 
panying map  is  only  intended  to  indicate  such  prevailing  kinds,  and 
of  course  each  color  covers  patches  of  greater  or  less  size,  of  different 
kinds. 

Notwithstanding  the  impracticability  of  mapping  these  local  varia- 
tions and  intermediate  varieties,  it  is  believed  that  the  map  given  will 


SOILS.  191 

prove  of  some  essential  service  to  the  increasingly  large  number  of 
our  agriculturists  who  desire  to  study  the  interests  of  their  professioii 
in  a  comprehensive  and  philosophic  manner.  The  following  descrip- 
tions will,  however,  be  found  quite  closely  applicable  in  detailed  study. 

CLASS  I.  Prairie  Loam.  This  class  is  too  well  known  to  need 
much  description.  It  sometimes  arises  from  the  decomposition  of 
the  underlying  limestone,  sometimes  from  the  disintegration  of  lime- 
stone gravel,  and  sometimes  it  arises  from  the  deposit  of  an  ancient 
lake.  There  are  several  varieties,  but  all  have  at  least  a  moderate 
degree  of  fineness  of  texture  while  some  manifest  this  quality  in  a 
very  high  degree.  This  is  more  particularly  true  of  those  that  are 
derived  directly  from  the  decomposition  of  the  limestone,  the  type  of 
which  is  a  black  "  light "  soil,  that  works  like  an  ash  bed  when  dry, 
and  rolls  into  little  pill-like  pellets  when  wet,  and  refuses  to  scour  ex- 
cept with  the  very  best  of  plows.  It  is  a  warm  soil,  but  not  so  rich 
as  its  blackness  might  lead  one  to  suppose,  yet  very  responsive  to 
proper  fertilizers.  This  particular  variety  occupies  but  limited  areas. 
The  other  kinds  are  slightly  more  arenaceous  and  work  with  the 
greatest  ease. 

In  chemical  composition,  silica  is  the  chief  ingredient,  with  which 
is  associated  a  variety  of  mineral  substances  that  constitute  plant  food, 
as  shown  by  the  analysis  at  the  close  of  these  descriptions. 

The  small  quantity  of  the  carbonates  of  lime  and  magnesia  may 
seem  at  first  strange,  since  the  soil  is  chiefly  derived  from  magnesian 
limestone,  but  it  becomes  clear  enough  when  we  consider  that  the 
disintegration  by  which  it  was  formed  consisted  of  the  dissolving  out 
of  the  lime  and  magnesia,  leaving  the  residue.  But  as  these  sub- 
stances exist  in  abundance  in  the  stratum  immediately  beneath,  and 
impregnate  the  water,  they  are  brought  to  the  surface  in  dry  weather 
by  capillary  action  so  that  these  soils  rarely  suffer  for  the  want  of 
mineral  substances.  In  judging  of  the  strength  of  our  soils  from 
analysis  it  should  be  borne  in  mind  that  there  exists  in  the  immediate 
substratum  an  inexhaustible  supply  of  the  soluble  mineral  substances 
needed  for  plant  food.  Our  soils  are  new  geologically  as  well  as  new 
in  the  history  of  cultivation. 

Vegetable  matter  in  the  form  of  humus  penetrates  this  soil  to 
greater  depths  than  in  most  of  the  following  classes,  and  imparts  to 
it  a  darker  color. 

The  areas  occupied  by  it  will  be  found  on  the  map  above  referred 
to.  It  will  be  observed  that  they  are  mainly  confined  to  the  south- 
western third  of  the  district  under  consideration,  or,  as  it  happens, 
perhaps  casually,  to  the  Mississippi  basin. 


192  GEOLOGY  OF  EASTERN  WISCONSIN. 

CLASS  II.  The  Lighter  Marly  Clay  Soils,  or  Clayey  Loams 
These  are  drift  soils,  having  been  derived  chiefly  from  a  calcareous 
bowlder  clay,  which  in  turn  was  formed  by  the  powdering  of  various 
kinds  of  rocks,  but  chiefly  magnesian  limestones,  by  glacial  agencies. 
It  therefore  contained  originally  a  large  proportion  of  calcareous  and 
magnesian  material,  and  a  less  amount  of  silicious  and  aluminous; 
but  the  leaching  action  of  water  and  the  growth  of  vegetation  has  re- 
moved a  much,  larger  amount  proportionally  of  the  lime  and  magne- 
sia than  of  the  other  ingredients,  so  as  to  leave  these  the  chief  con- 
stituents at  the  surface.  But  the  deeper  subsoil  is  highly  marly  in 
its  nature.  There  is  just  enough  of  sandy  material  in  it  to  make  it 
loamy.  The  dark  vegetable  matter  does  not  penetrate  as  deeply  as  in 
the  prairie  loam,  so  that  the  plow  frequently  turns  up  the  reddish  or 
yellowish  subsoil  containing  very  little  humus.  This  soil  works  with 
the  utmost  facility,  indeed  is  unsurpassed  in  this  respect.  It  stands 
both  wet  and  drought  well,  and  is  a  very  durable  and  fertile  soil. 

This  class  graduates  into  the  sandy  loams  on  the  one  hand,  and 
heavier  clayey  loams  on  the  other.  It  prevails  in  the  same  general 
region  as  the  prairie  loams,  its  areas  being  irregularly  interwoven 
with  them. 

CLASS  III.  The  Heavier  Merely  Clay  Soils,  or  Heavier  Clayey 
Loams.  This  class  is  similar  to  the  preceding,  both  in  origin  and 
character.  But  the  drift  from  which  it  was  derived  contained  more 
Archaean  bowlders,  especially  those  containing  feldspar,  hornblende, 
and  similar  minerals  in  large  proportion.  From  the  powdering  and 
disintegration  of  these,  a  large  amount  of  clay  proper  was  derived, 
mingled,  however,  with  the  quartzose  material  of  the  same  rocks  and 
with  much  calcareous  and  magnesian  clay,  derived  in  a  similar  way 
from  the  -dolomites  which  usually  form  a  prominent  part  of  the  drift. 
This  is  not  then  a  true  clay  soil,  for  there  is  a  notable  proportion  of 
lime,  magnesia  and  free  silica  present,  but  it  is,  as  named  above,  a 
marly  clay,  of  the  heavier  class,  when  compared  with  the  foregoing. 
The  term  loam  is  not  properly  applicable  to  the  subsoil,  but  at  the 
surface,  drainage  has  exercised  an  assorting  influence  over  it,  separat- 
ing and  carrying  away  the  finer  material,  and  leaving  the  sand,  which 
gives  to  the  surface  a  lighter  loamy  character.  This  surface  soil 
rarely  gives  any  effervescence  when  submitted  to  the  action  of  hydro- 
chloric acid,  while  that  from  greater  depths  usually  responds  with 
vigorous  action.  We  find  here  again  what  I  have  found  to  be  true 
everywhere,  that  the  surface  soil  is  almost  entirely  exhausted  of  the 
carbonates  of  lime  and  magnesia,  even  where  they  exist  in  gxeat 
abundance  in  the  deeper  subsoil.  And  it  is  for  this  reason  that  tiie 


SOILS.  193 

origin  and  nature  of  the  comparatively  unmodified  subsoil  must  be 
studied  if  we  are  to  arrive  at  any  reliable  conclusions  as  to  the  per- 
manent resources  of  our  soils.  A  considerable  proportion  of  iron 
exists,  as  might  be  expected,  from  the  decomposition  of  the  horn- 
blende and  allied  minerals,  and  gives  to  the  soil  a  yellowish  orange  or 
reddish  color.  The  high  color  indicates  the  presence  of  the  sesquiox- 
ides;  and  the  more  or  less  chalybeate  character  of  the  waters  demon- 
strates the  existence  of  the  more  soluble  compounds;  while  a  magnet 
drawn  through  the  pulverized  soil  frequently  brings  forth  a  bristling 
edge  of  magnetite,  showing  the  presence  of  iron  in  that  form.  The 
surface  is  frequently  strewn  with  bowlders,  chiefly  "hard-heads," 
while  cobble  stones  and  pebbles  mingle  more  or  less  with  the  soil, 
though  not  to  an  extent  that  would  often  justify  the  term  gravelly. 
The  vegetable  mold  is  confined  mainly  to  a  few  inches  at  the  surface. 

This  soil  works  with  more  difficulty  than  the  last,  but  is  strong  and 
enduring,  and  will  improve  rather  than  otherwise  with  use.  It  be- 
comes lighter  and  warmer  as  it  is  stirred,  and  is  gradually  becoming 
fitted  for  crops  that  did  not  at  first  flourish  upon  it.  This  is  the  pre- 
vailing soil  in  the  heavily  timbered  regions  in  the  central  portions  of 
our  district. 

CLASS  IY.  The  Red  Marly  Clay  Soils.  The  term  "  red  clay  "  is 
popularly  applied  to  a  very  extensive  deposit  in  the  northeastern 
part  of  the  state,  and  to  the  soil  derived  from  it.  It  is  very  properly 
denominated  a  clay,  if  we  use  the  term  in  a  simply  physical  sense.  It 
is  finely  comminuted,  close,  compact,  adhesive  and  almost  impervious. 
It  washes,  cracks  and  otherwise  deports  itself  as  a  clay.  These  qual- 
ities, however,  do  not  reach  an  excessive  development.  It  never  pos- 
sesses that  extreme  tenacity  when  wet,  or  that  obdurate  hardness 
when  dry,  that  characterizes  the  typical  aluminous  clay.  It  contains, 
moreover,  in  most  localities,  fragments  of  limestone,  and  occasionally 
other  rock,  which  modify  these  qualities.  In  chemical  composition, 
however,  it  is  not  a  true  clay.  Beside  the  aluminous  element,  there 
is  a  varying  proportion  of  silicious  matter,  a  notable  ingredient  of 
carbonate  of  lime  and  magnesia,  and  a  very  constant  intermixture  of 
hematite  and  magnetite.  It  is  rarely  that  a  magnet  drawn  through 
a  handful  of  dust  fails  to  bring  forth  grains  of  the  latter.  In  like 
manner  the  application  of  acid  to  the  unleached  subsoil  seldom  fails 
to  give  a  prompt  and  vigorous  effervescence.  The  opposite  is  true, 
however,  of  the  surface  soil.  The  difference  between  the  two  is  also 
usually  indicated  by  physical  characteristics.  One  of  the  most  no- 
ticeable of  these  is  the  intimate  fissuring  of  the  upper  subsoil  when 
dry,  by  innumerable  little  cracks  that  divide  the  mass  into  small  rude- 
Wis.  SUR.— 13 


194:  GEOLOGY  OF  EASTERN  WISCONSIN 

ly  cubical  blocks,  so  that  when  dug  up  it  is  neither  pulverulent  nor 
aggregated  in  rounded  clods,  as  is  the  case  with  arenaceous  and  loamy 
soils,  but  is  simply  a  heap  of  little  blocks.  From  this  portion  the 
carbonates  have  been  pretty  thoroughly  removed.  Hydrochloric  acid 
seldom  produces  effervescence,  never  any  vigorous  action.  The  fissur- 
ing  is  to  be  regarded  as  the  cause  rather  than  as  the  result  of  this  re- 
moval of  the  soluble  carbonates.  The  color  of  this  portion  is  also 
somewhat  duller  and  more  inclined  to  a  mottled  and  brownish  hue 
than  the  lower  unmodified  portion,  which  is  usually  a  pinkish  or  pur- 
plish red.  This  lower  portion  is  the  true  subsoil,  and  is  the  part 
previously  described.  The  immediate  surface  has  an  ash  color. 

This  soil  needs  thorough  working,  which  is  not  so  easily  accom- 
plished as  with  the  loamy  arenaceous  soils,  but  it  yields  excellent  re- 
turns. It  is  an  exceedingly  strong,  durable,  fertile  soil.  Its  strength 
lies  in  its  native  constitution  and  not  in  a  superficial  layer  of  vegeta- 
ble mold,  soon  to  be  exhausted.  Cultivation  improves  rather  than 
exhausts  it,  and  it  will  still  continue  to  yield  bountiful  harvests  when 
many  other  soils  will  need  the  constant  stimulus  of  fertilizers.  The 
stirring,  the  washing  out  of  the  finer  materials,  and  the  exposure  to 
the  air  incident  to  cultivation,  give  it  a  lighter  and  warmer  character, 
so  that  after  a  few  years  cultivation,  crops  may  profitably  be  intro- 
duced that  at  first  were  unsuccessful. 

The  map  shows  it  to  occupy  a  belt  along  Lake  Michigan,  from  Mil- 
waukee to  Sturgeon  Bay,  widening  to  the  northward  until  it  passes 
the  summit  between  the  lake  and  the  great  valley,  and  occupies  the 
basin  of  the  Fox  river  and  Lake  Winnebago. 

CLASS  Y.  The  Limestone  Loam.  This  is  not  a  very  sharply  de- 
fined class.  It  appears  to  have  its  origin  in  the  decomposition  of  the 
magnesian  limestone  upon  which  it  rests.  It  thus  differs  from  either 
of  the  marly  clays,  to  which  it  is  most  nearly  allied,  in  not  being  a 
drift  soil.  It  is  usually  yellowish  or  reddish  in  color,  rather  plastic 
and  adhesive,  moderately  comminuted,  of  only  medium  porosity,  and 
in  chemical  nature  it  is  chiefly  silicious  and  aluminous,  or  in  the  lan- 
guage of  its  origin,  the  insoluble  residue  of  the  limestone.  The  car- 
bonates of  lime  and  magnesia,  though,  forming  the  chief  constituents 
of  the  original  rock,  are  present  in  the  soil  in  very  limited  quantities. 
This  makes  the  use  of  the  name  here  given  objectionable,  if  it  is 
thought  to  indicate  the  composition  of  the  soil.  It  was  selected  for 
want  of  a  better  one  to  indicate  its  origin. 

The  depth  of  the  soil,  except  in  the  valleys,  is  not  considerable,  and 
the  rock  itself  is  really  to  be  regarded  as  the  permanent  subsoil.  It  is 
reached  even  by  the  roots  of  cereals  over  much  of  the  area  occupied 


SOILS.  195 

by  this  class.     It  is  a  fertile  soil,  is  easily  worked,  and  supports  a 
dense  growth  of  timber. 

CLASS  VI.  Silicious  Sandy  Soils.  This  class  needs  little  atten- 
tion here,  because,  in  the  first  place,  it  is  too  well  known  to  require 
elaborate  definition,  and,  in  the  second  place,  it  fortunately  occupies 
so  little  area  that  it  posseses  no  great  importance  in  considering  the 
district  as  a  whole.  As  found  in  this  region,  it  had  its  origin  in  beach, 
deposits  made  by  the  lake  in  former  times,  and  in  drift  from  silicious 
rocks.  As  it  occurs  chiefly  in  narrow  strips  surrounded  or  bordered 
by  clay  soils,  it  may  not  on  the  whole  prove  a  great  disadvantage, 
although  of  itself  it  is  a  sterile  soil,  for  when  it  mingles  with  the 
adjoining  clay  it  produces  a  rich,  fertile  loam,  better  adapted  to  some 
crops  than  the  clays  themselves. 

CLASS  VII.  The  Calcareous  Sandy  Soils.  My  attention  was  first 
called  to  this  class  by  observing  a  heavy  growth  of  maple  and  associ- 
ated trees  upon  a  sandy  soil.  This  was  so  contrary  to  previous  obser- 
vations that  it  led  to  an  examination  of  the  sand.  This  showed  it  to 
be  composed  of  small  crystals  of  dolomite  mingled  with  a  varying 
quantity  of  silicious  grains.  From  the  immediate  surface  the  more 
soluble  dolomite  has  been  removed,  leaving  the  silicious  sand  at  the 
top  in  such  a  way  as  to  disguise  the  true  nature  of  the  subsoil.  This 
surface  soil  is  light,  warm  and  arenaceous,  but,  to  casual  observation, 
would  give  no  promise  of  permanent  fertility.  The  fact  that  the  sub- 
soil is  so  largely  dolomitic,  instead  of  silicious,  adds  not  less  than 
one  hundred  per  cent,  to  the  value  of  the  land.  A  general  knowledge 
of  this  fact  on  the  part  of  the  proprietors  ought  not  only  to  add  to  the 
appreciation  in  which  their  land  is  held,  but  enhance  their  returns  by 
guiding  them  in  selecting  those  crops  for  which  their  soil  is  peculiarly 
adapted.  This  also  presents  a  rich  field  for  the  study  of  agricultural 
problems  relating  to  sandy  and  calcareous  soils.  This  is  not,  however, 
the  sole  occupant  of  any  considerable  area,  but  is  freely  intermingled 
with  marly  clay  and  gravelly  soils  and  various  intermediate  grades,  as 
well  as  the  silicious  variety.  It  is  a  drift  soil.  The  calcareous  sand 
had  its  origin  in  the  granular  dolomites  of  the  Niagara  Group. 

CLASS  VIII.  The  Humus  Soils.  Under  this  head  is  grouped 
those  soils  in  which  humus  in  some  of  its  varieties,  chiefly  peat  and 
swamp  muck,  is  the  predominant  element,  and  in  which  the  mineral 
ingredients  are  largely  concealed  by  it.  The  peaty  soils  are  the  type 
of  the  class.  In  these,  not  only  the  surface  but  the  subsoil  is  chiefly 
of  organic  origin.  Soils  simply  covered  with  a  layer  of  vegetable  mold 
are  not  here  included.  Almost  all  the  swampy,  and  a  large  portion  of  the 
bottom  lands,  are  covered  by  this  soil.  But  it  is  not  so  easy  to  define 


196 


GEOLOGY  OF  EASTERN  WISCONSIN. 


the  adaptabilities  of  this  class,  or  measure  its  fertility.  Some  por- 
tions, with  simple  drainage,  will  produce  the  most  luxuriant  growth 
of  grass  or  grain.  Others  are  impregnated  with  organic  acids  derived 
from  the  humus,  and  are  known  as  "  sour  soils,"  and  are  unfit  for  the 
growth  of  the  cereals  and  the  better  class  of  grasses.  Others  still  are 
so  largely  composed  of  organic  matter  that  they  do  not  contain  the 
requisite  amount  of  mineral  ingredients.  The  character  of  the  vege- 
tation naturally  growing  upon  it  is  the  best  indication  of  the  nature 
of  any  given  example  of  this  class. 

Alluvial  Soils.  Closely  associated  with  this  last  class,  and  inter- 
mediate between  it  and  the  prairie  loam,  we  find  a  soil  formed  by  the 
accumulation  of  sediment  washed  from  the  uplands  and  deposited  on 
the  bottom  lands  adjacent  to  streams,  and  in  other  favorable  localities. 
It  is  better  marked  in  its  origin  than  in  its  character,  for  when  min- 
eral ingredients  predominate,  it  very  closely  resembles  the  prairie 
loam,  both  in  the  fineness  of  the  material  and  in  its  chemical  nature, 
and  when  vegetable  matter  becomes  predominant  it  does  not  differ 
essentially  from  the  humus  soils.  For  this  reason,  and  because  its 
distribution  has  no  special  significance  in  studying  agricultural  prob- 
lems, it  has  not  been  mapped  as  a  separate  class,  although  it  occupies 
in  the  aggregate  a  large  area,  and  is  an  exceedingly  fertile  and  valu- 
able soil.  The  following  analyses  are  by  Mr.  Bode: 


ANALYSES  OF  SOILS. 

100  PAKTS  OF  THE  DRIED  SOIL 
CONTAIN 

Prairie  loam 
from  south 
central  Wis. 

rS  -4J  oa 

TO  Orc 

|ga 

Hi 

Soluble  in  hydrochloric  acid  — 

4.24 
2.88 
2.34 
0.60 
0.18 
0.18 
0.04 
0.49 
0.19 
0-06 
0.52 
0.03 

78.99 
5.28 
1.12 
1.03 
1.83 

21.40 
3.59 
2.52 
0.07 
0.13 
0.28 
0.03 
0.51 
0.14 
0.12 
0.25 
0.08 

64.42 
2.15 
1.34 
0.69 

2.28 

5.84 
3.03 
2.82 
0.50 
0.12 
4.02 
3.48 
0.15 

Oxide  of  iron    .'  

Alumina  

Silica  

.Magnesia  

Potassa    

Phosphoric  acid  

0.19 

7.08 
0-02 

59.76 
1.36 
1.01 

Sulphuric  acid  

Insoluble  in  hydrochloric  acid  — 

Oxide  of  iron  

10.62 

100.00 

100.00 

100.00 

SOILS.  ]  97 

J\£agiiesian  Character  of  these  Soils.  It  is  worthy  of  notice  liere 
that  these  soils  are  magnesian.  This,  I  believe,  in  the  future  unf old- 
ings  of  agricultural  science,  will  be  found  to  be  a  very  important  fact. 
Magnesia  has  been  a  much  abused  substance.  It  was  formerly  sup- 
posed that  magnesian  limestone  made  an  inferior  quick  lime,  and  it 
long  lay  under  disfavor.  But  experience  has  finally  shown  that  pre- 
cisely the  opposite  is  true.  It  is  far  superior  to  pure  limestone  for  this 
purpose.  It  was  long,  indeed  almost  even  now,  thought  to  be  unsuited 
for  flux  with  iron  ores,  but  this  opinion  has  recently  been  modified. 
Magnesian  limestone,  burned  to  quicklime,  was  formerly  prohibited 
as  a  fertilizer,  and  the  ban  has  been  only  recently  removed.  That 
some  such  revolution  of  opinion  must  take  place  in  reference  to  its 
utility  as  an  ingredient  of  the  soil  seems  to  be  forcibly  suggested  by 
the  following  extracts  from  analyses  taken  from  Prof.  Johnson's  ex- 
cellent treatise  "  How  Crops  Grow,"  "  being  the  average  of  all  trust- 
worthy analyses  published  up  to  August,  1865  ": 

MAGNESIA.    LIME. 
Per  cent.    Per  cent. 

Wheat 12.2  3.1 

Rye 10.9  2.7 

Barley   8.3  2.5 

Oats 7.3  3.8 

Maize - 14.6  2.7 

Buckwheat 13.4  3.3 

Flax 13.2  8.4 

Beet 18.9  15,6 

Turnip 8.7  17.4 

CaiTot 6.7  38.8 

Peas 8.0  4.2 

Field  beans 6.7  5.2 

Garden  beans 7.5  7.7 

Clover  seed 12.2  6.2 

Potatoes 4.5  2.3 


From  which  we  see  that  in  the  grains,  the  magnesia  predominates 
decidedly.     In  the  fibrous  part  of  the  plant  the  opposite  is  true;  as 

follows : 

MAGNESIA.    LIME. 
Per  cent.    Per  cent. 

Winter  wheat  straw 2.6     •        6.2 

Bye 3.1  7.7 

Barley 2.4  7.6 

Oats 4.0  8.2 

Maize 5.5  10.5 

Peas 7.7  37.9 

Field  beans -7.8  23. 1 

Garden  beans 5.2  27.4 

Buckwheat 3.6  18.4 


198  GEOLOGY  OF  EASTERN  WISCONSIN. 

MAGNESIA.    LIME. 

Per  cent  Per  cent. 

Oak,  body  wood 4.8  73.5 

Oak,  small  branches  with  bark 7.5  54.0 

Poplar,  young  twigs 7.5  58 . 4 

Elm,  young  twigs 10.0  37.9 

Elm,  body  woo d 7.7  47.8 

Linden  (Bass  wood) 4.2  29.9 

Apple  tree 5.7  81.0 

Apple  tree,  entire  fruit 8.8  4.1 

Beech 45.8  16.8 

White  pine 5-9  50.1 

Larch 24.5  27.1 

The  percentages  relate  to  the  ash  of  the  plant. 

For  other  facts  of  similar  import,  see  the  work  cited  above.  These 
facts  go  to  show  that  magnesia  is  more  concerned  in  fruit  produc- 
tion, and  lime  in  the  formation  of  fiber.  In  view  of  this  it  may  be  asked 
whether  the  well  known  superiority  of  Wisconsin  wheat  is  not  due  to 
the  magnesiaii  element  in  her  soils. 

If  we  compare  the  map  of  soils  with  the  map  of  vegetation  we 
shall  find  some  interesting  and  important  relations.  The  Prairie 
Loam  is  of  course  covered  by  prairie  vegetation.  The  Lighter 
Marly  Clays  are  chiefly  occupied  by  the  oak  group,  the  Heavier  Mar- 
ly Clays  by  the  vegetal  groups  in  which  the  maples  are  prominent, 
The  Red  Marly  Clay  by  very  much  the  same;  the  Limestone  Loam 
by  the  maple,  beach  and  conifers  in  the  peninsula  and  chiefly  by  the 
oaks  elsewhere,  this  difference  being  due  probably  to  climatal  influ- 
ences; the  Silicious  Sandy  soils  by  the  conifers  chiefly ;  the  Calcareous 
Sandy  soils  by  the  maple  and  oak  and  the  maple  and  beech  groups. 
The  Humus  soils  are  occupied  by  the  several  classes  of  swamp  vege- 
tation. Where  a  patch  of  heavy  clay  occurs  in  an  area  of  the  lighter 
class  it  usually  sustains  heavy  oak  timber,  especially  white  oak, 
rather  than  the  "  openings,"  and  where  the  reverse  is  true,  the  oak 
and  maple  group  usually  displaces  the  other  maple  groups.  The 
pine  is  frequently  found  on  soils  that  are  quite  decidedly  clayey  in 
nature,  but  in  many  of  these  cases  a  substratum  of  sand  is  to  be  found 
within  a  few  feet  of  the  surface. 

These  correspondences,  which  are  susceptible  of  being  carried  out 
to  much  greater  detail,  illustrate  the  mutual  relations  of  soil  and  na- 
tive vegetation,  and  open  to  the  agriculturist  a  wide  field  for  profit- 
able study. 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  199 


CHAPTER  Y. 
QUATERNARY  FORMATIONS  —  THE   DKIFT. 

The  formations  of  this  region  consist  of  two  great  classes,  the  one 
made  up  of  indurated  rock,  the  other  of  loose  material  in  the  form  of 
clay,  sand,  gravel  and  bowlders.  The  former  had  their  origin  in  de- 
posits made  by  the  ancient  ocean,  which  have  become  hardened  to  the 
state  in  which  we  now  find  them.  The  others  had  their  primary  ori- 
gin, as  is  now  generally  believed,  in  the  action  of  ice  in  the  form  of  a 
glacier.  Subsequently  a  large  portion  of  this  material  was  washed. 
out  and  redeposited  or  otherwise  modified  by  the  action  of  lakes  and 
rivers.  That  portion  which  remains  in  the  condition  in  which  it  was 
originally  left  by  the  glacier  is  known  as  unmodified  drift,  while  that 
which  has  been  rearranged  and  redeposited  by  the  subsequent,  action 
of  water  is  termed  modified  drift.  Taken  together,  they  constitute 
the  chief  Quaternary  formations.  Since  they  occur  at  the  surface  and 
are  diverse  from  the  bedded  rocks  below,  in  their  nature  and  origin, 
it  will  be  most  convenient  to  consider  them  independently. 

The  primary  drift,  or  that  portion  of  the  material  which  exists  in 
the  condition  in  which  it  was  left  on  the  retreat  of  the  glacier,  will 
be  considered  under  the  head  of  (1)  moraine  ridges,  and  (2)  bowlder 
clay  or  till.  The  secondary  or  modified  drift  consists  of  a  series  of 
beach  deposits  of  sand  and  gravel,  and  of  lacustrine  deposits  of  clay. 
In  addition  to  these  there  are  many  local  deposits  made  by  running 
streams  and  small  lakes  that  will  not  receive  special  consideration. 

Glacial  Movements.  To  clearly  understand  these  drift  formations, 
it  will  be  desirable  to  first  study  the  character  of  the  glacial  move- 
ments which  gave  rise  to  them.  At  the  commencement  of  the  great 
cold  period  which  led  to  the  vast  accumulations  of  ice  which  over- 
spread this  portion  of  the  continent,  this  part  of  Wisconsin  had 
already  been  long  elevated  above  the  surface  of  the  ocean,  and  had 
been  subjected  to  very  great  erosion,  by  which  extensive  and  deep  val- 
leys had  been  formed.  There  can  be  no  doubt  that  the  Green  Bay  and 
Rock  River  valleys  were  already  in  existence,  though  doubtless  pre- 
senting many  features  very  different  from  those  exhibited  at  the^  res- 
ent time.  There  is  abundant  evidence  that  some  of  the  streams  had 


200  GEOLOGY  OF  EASTERN  WISCONSIN. 

cut  channels  from  one  to  three  hundred  feet  deeper  than  those  which 
they  now  occupy.  These  preexisting  features  of  the  surface,  exerted 
a  very  marked  and  peculiar  influence  upon  the  direction  of  glacial 
movement. 

FIG.  2. 


A  striated  half-cone  of  rock  on  a  glaciated  surface  of  limestone,  seen  at  Pelton's  quarry,  Pewnn- 
kee.  The  parallel  lines  represent  the  strife  .  The  base  of  the  cone  is  not  striated  and  the  adjacent 
surface  is  at  first  rough,  but  becomes  gradually  smoothed,  and  at  length  merges  into  the  polished 
plane  surface,  demonstrating  the  direction  of  glacial  movement. 

In  its  progress  the  ice  mass  abraded  the  surface  of  the  rock,  carry- 
ing away  and  grinding  up  the  material  detached,  and  by  means  of  it, 
embedded  in  its  base,  polishing  and  scoring  the  ledges  below,  there- 
by indicating  the  direction  of  its  movement,  and  leaving  us  its  own 
history  engraven  on  the  surface  of  the  rock.  By  careful  observation 
of  these  scratches  or  strise,  it  has  been  found  possible  in  all  except  a 
few  cases  to  tell  the  point  of  compass  towards  which  the  movement 
took  place.  By  such  observations  it  appears  that  the  movements  of  the 
ice  in  this  region  were  of  an  exceedingly  interesting  character.  On 
the  east  side  of  the  Kettle  Range,  with  some  unimportant  exceptions, 
the  direction  of  movement  was  in  a  westerly  or  southwesterly  direc- 
tion, or  towards  the  Range.  The  exceptions  are  cases  in  which  two 
sets  of  strias  are  present,  the  one  set  corresponding  to  the  general  di- 
rection just  indicated,  the  other  to  the  general  trend  of  Lake  Michi- 
gan. On  the  other  side  of  the  Kettle  Range,  between  it  and  the  crest 
of  the  ledge  that  borders  the  Green  Bay  valley,  heretofore  described, 
the  direction  is  to  the  southeasterly  toward  the  Kettle  Range.  With- 
in the  great  Green  Bay  valley  the  direction  is  uniformty  parallel  to 
its  trend,  and  the  cutting  and  planing  indicates  a  long  continued  and 
powerful  action.  To  the  west  of  this  valley,  the  striae  have  a  west- 
ward and  southwestward  direction,  the  tendency  being  in  general 
more  to  the  westward  as  the  slope  is  ascended.  It  appears  then  that 
the  movement  on  the  east  side  of  the  Kettle  Range  was  up  the  slope 
obliquely  towards  it;  that  on  the  west  side  of  the  Range,  between  it 
and  the  margin  of  the  Green  Bay  valley,  the  movement  was  obliquely 
down  the  slope  toward  the  Range ;  that  within  the  Green  Bay  valley 
the  ice  moved  up  it  until  it  reached  the  dividing  ridge  between  it  and 
the  Rock  River  valley,  when  it  descended  the  latter,  the  lines  gradu- 


QUATERNARY  FORMATIONS— THE  DRIFT.  201 

ally  diverging  as  it  did  so;  and  that  on  the  west  side  of  the  valley,  tho 
movement  was  again  up  the  slope,  and  gradually  divergent.  Over  the 
Green  Bay  peninsula,  striatious  are  very  rare,  on  account  of  the  ab- 
sence of  conditions  favorable  to  their  preservation,  but  there  is  un- 
questioned evidence  that  the  movement  was  obliquely  across  the  penin- 
sula/Vcw  the  Green  Bay  valley  to  the  trough  of  Lake  Michigan.  In 
the  following  table  the  strias  have  been  classified  with  reference  to 
these  general  movements : 

I.  —  BET-WEEK  THE  KETTLE  RANGE  AND  LAKE  MICHIGAN. 

Horlick's  quarry,  Racine  (doubtful), S.  26°  W. 

Schwickhart's  quarry,  Sec.  26,  N.  W.  qr.,  "Wauwatosa S.  49°  W. 

Sheboygan  Falls,  village S.  64°  W. 

Sheboygan  Light-house  — 

First  set S.  56°  W. 

Second  set S.  41  W. 

Howard's  quarry,  Sec.  16,  Sheboygan  Falls S.  78°  W. 

Kuntz'  quarry,  on  Manitowoc  river,  Sec.  15,  Manitowoc  Rapids S.  81°  W. 

One  half  mile  below  the  above,  Sec.  15,  Manitowoc  Rapids S.  79°  W. 

Moody's  quarry,  4th  Ward,  Milwaukee S.  86°  W. 

Pelton's  quarry,  Pewaukee  S.  82°  W. 

Udafield,  Sec.  20,  S.  E.  qr S.  1161  W. 

Pewaukee,  Sec.  18,  N.  W.  qr S.  92C  W. 

Lisbon,  Sec.  35 S.  96°  W. 

II.  —  BETWEEN  THE  KETTLE  RANGE  AND  THE  GREEN  BAT  AND  •  ROCK  RIVER 

VALLEY. 

Casco,  Sec.  14,  S.  W.  qr.,  T.  24,  R.  23,  on  summit  of  ridge S.     4"  E. 

"      on  east  brow  of  the  ridge,  on  top  and  edge  of  layer S.  21°  W 

Marshfield,  J.  Steffer's  quarry,  Sec.  30,  S.  W.  qr S.  28°  E. 

Taycheedah,  T.  16,  R.  18,  Sec.  29,  S.  W.  qr.  of  S.  E.  qr S.  10°  E. 

Empire,  Sec.  5,  N.  W.  qr S.  18°  E. 

Ashford,  R.  R.  cut,  Sec.  11 S.  59"  E. 

Elmore,  Ashford,  Sec.  26,  N.  E.  qr S.  44°  E. 

Whitewater,  near  Krnney's S.     7°  E. 

Whitewater,  S.  E.  of  Cravath  lake S.  12°  W. 

III. — IN  THE  TROUGH  OF  THE  GREEN  BAY  AND  ROCK  RIVEB  VALLEY. 

Ft.  Howard,  Sec.  10,  Bennett's  quarry,  Duck  creek S.  29"  W. 

"  "          North  quarry S.  20°  W. 

Peshtigo,  T.  30,  R.  22,  Sec.  4,  near  center S.  41°  W. 

Peshtigo,  T.  30,  R.  22  E.,  Sec.  21,  E.  hf.  S.  W.  qr. S.  27°  W. 

Oneida  Reserve,  mill  on  Duck  creek S.   20"  W. 

Menasha,  Sec.  11,  E.  hf.  of  S.  W.  qr S.  2H°W 

Neenah,  Sec.  34,  N.  E.  qr S.  27°  W. 

Fond  du  Lac,  Moore's  quarry S.   15°  "W. 

Taycheedah S.   15°  W. 

Byron,  Sec.  10 S.     3°  W. 

Beaver  Dam,  Sec.  20,  S.  E.  qr due  south. 

Koshkonong  Prairie S.     7°  E. 

Fulton,  Sec.  12,  N.  E.  qr S.   13°  W. 


202 


GEOLOGY  OF  EASTERN  WISCONSIN. 


III.  —  Ox  THE  WEST  SLOPE  OF  THE  GREEK  BAY  AND  ROCK  RIVER  VALLEY. 

Portland,  Sec.  35,  S.  E.  qr S.  30°  W. 

Milford,  Sec.  33,  S.  W.  qr S.  30°  W. 

Calamus,  Sec.  18,  near  center S.  36°  W. 

Westford,  Sec.  19,  middle  S.  E.  qr.  — 

First  set S.   24°  W. 

Crossed  by  second  set S.  46°  W. 

Trenton,  McFarland's  quarry S.  50°  W. 

Green  Lake,  Sec.  36 S.  45°  W. 

Green  Lake,  Sec.  3 due  west. 

Ripon,  Sec.  19 S.  82°  W. 

Metomen,  Sec.  1,  N.  E.  qr S.  45°  W. 

Nepeuskin,  Sec.  4,  near  middle  south  line S.  94°  W. 

Nepeuskin,  Sec.  15,  N.  W.  qr S.  87°  W. 

Nepeuskin,  Sec.  15,  near  center S.  84°  W. 

Black  Creek,  watering  station  G.  B.  &  M.  R.  R S.  72°  W. 

Peshtigo,  T.  33,  R.  20,  Sec.  21,  E.  hi  of  S.  W.  qr S.  82°  W. 

FHJ.  3.  IV.  —  GREEN  BAY  PENINSULA,  FIORD  REGION. 

Liberty  Grove,  T.  31,  R.  28  E.,  Sec.  25,  near  North  Bay. 

First  set S.     9°  E. 

Crossed  by  second  set S.    4°  E. 

Besides  the  striae,  there  is  abundance  of 
evidence  from  other  sources,  testifying  to 
these  movements.  Where  Archaean  mass- 
es protrude  through  the  Paleozoic  forma- 
tions, as  in  the  towns  of  Berlin,  Marquette, 
Green  Lake,  Portland  and  Waterloo,  trains 
of  bowlders  stretch  away  from  them  in  the 
direction  of  glacial  motion.  In  the  latter 
case  these  trains  have  been  traced  to  the 
southern  line  of  the  state,  50  miles  distant, 
as  illustrated  in  the  accompanying  map. 

Evidence  of  a  similar  nature,  though  less 
conspicuous,  is  furnished  by  drift  from 
peculiar  beds  of  Paleozoic  formations. 
In  addition  to  this,  the  contour  of  the  rock  surface  furnishes  cor- 
roborative testimony.  Elongated  domes  of  rock  having  a  linear  ar- 
rangement, with  their  longer  axes  parallel  to  each  other,  indicate  the 
direction  of  the  moving  ice.  In  the  same  way  elongated  drift  hills 
and  ridges,  often  of  a  very  great  length,  indicate  the  direction  of 
movement,  either  because  they  lie  in  it,  in  which  case  they  have  a 
rounded,  flowing  contour,  or  because  they  lie  transverse  to  it,  in 
which  case  they  usually  have  a  sharp  or  irregular  outline.  On  the 
east  side  of  the  Kettle  Kange,  in  the  region  of  southwestward-point- 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  203 

ing  striae,  the  rock  ridges  and  drift  ridges  of  flowing  outline  have  a 
westerly  or  southwesterly  trend.  On  the  west  side  of  the  Range  and 
adjacent  to  it,  they  have  a  southerly  or  southeasterly  inclination.  In 
the  upper  portion  of  the  Rock  River  valley,  they  are  often  exceedingly 
conspicuous  in  their  southerly,  southeasterly  or  southwesterly  trend 
according  to  their  position  within,  on  the  east,  or  on  the  west  of  the 
main  line  of  glacial  movement.  The  persistency  and  uniformity  of 
this  arrangement  in  Dodge  and  Jefferson  counties  is  something  re- 
markable. As  will  be  observed,  in  all  these  cases,  the  arrangement 
of  this  class  of  drift  hills  corresponds  to  the  direction  of  the  glacial 
grooves. 

In  this  connection  we  need  to  consider  some  peculiar  phenomena, 
that  occur  at  Mr.  Smith's  quarry,  near  Burlington,  and  at  Mr.  Cas- 
tleman's,  in  East  Troy.  The  position  of  these  quarries  is  such  as  to 
make  the  following  facts  of  much  interest  in  relation  to  the  Kettle 
Range,  aside  from  that  pIG  ^ 

which  attaches  to  them  in- 
dependently. The  accom  • 
panying  sketch  represents 
a  vertical  section  along  the 


Ri'rlp  nf  Smifl-i'«  nnirrv       a.  Solid  beds  of  limestone.    6.  Study  beds.    c.  Thick  layer 
S  qUciriy.  iime8tone  fractured  at  the  left.    d.  Drift  containing 

The  upper  four  or  five  feet       tnted  blocks  of  limestone. 

consist  of  soil  and  debris  resting  upon  the  regularly  bedded  argilla- 
ceous limestone.  The  upper  portion  of  the  loose  material  is  a  marly 
clay  of  dark  reddish  brown  color,  and  partly  stratified.  The  lower 
portion  is  made  up  of  fragments  of  the  limestone  that  forms  the  body 
of  the  quarry,  imbedded  in  sand,  clay,  and  gravel.  The  blocks  of 
limestone  are  angular  and  unworn,  and  sometimes  not  even  separated, 
from  the  layers  with  which  they  were  contiguous  before  disturbance. 
They  are  almost  uniformly  tilted,  so  as  to  dip  at  high  angles  toward 
the  south  or  southwest,  as  represented  in  the  figure.  The  number  of 
the  titled  blocks  is  so  great,  and  their  position  so  constant,  that  the 
phenomena  cannot  be  regarded  as  a  mere  chance  occurrence. 

The  surface  of  the  undisturbed  rock  is  frequently  smoothed,  but 
no  distinct  striae  could  be  found.  On  the  opposite  side  of  White 
river,  five  or  six  rods  distant,  the  surface  is  thoroughly  smoothed,  but 
presents  no  striae,  and  although  planed  to  a  general  level,  undulat- 
ing portions  are  smoothed  in  a  way  not  readily  attributable  to  ice. 
Taken  altogether,  the  phenomena  seem  to  point  to  original  polishing 
by  glacial  agencies,  and  subsequent  modification  by  water. 

In  the  northern  part  of  the  quarry,  the  strata  are  removed  to  a 
lower  level.  The  upper  layer  represented  in  the  sketch  is  firm  and 


204  GEOLOGY  OF  EASTERN  WISCONSIN. 

compact,  but  fractured,  as  shown.  Just  below  this  lies  a  softer  and 
more  yielding  shaly  layer.  At  the  left,  where  unprotected  by  the 
layer  above,  it  is  sharply  arched.  Unfortunately,  debris  obscured  the 
section  beyond  this  point.  Enough,  however,  was  removed  to  show 
all  the  essential  features. 

At  Castlernan's  quarry  the  loose  pieces  were  tilted  more  irregularly, 
but  the  surface  of  the  rock  is  smoothed,  and  some  obscure  striae  are 
to  be  found  whose  direction  is  S.  45°  to  50°  "W. 

The  combined  import  of  these  facts  is,  that  the  force  producing  the 
phenomena  acted  from  the  northeast.  This  demonstration  is  the 
more  important  since  we  have  little  other  evidence  of  a  decisive  na- 
ture relating  to  the  direction  of  glacial  movement  in  this  region.  But 
such  evidence  as  can  be  derived  from  the  drift  and  topography  cor- 
roborates this  conclusion. 

The  combined  testimony  of  these  several  witnesses  establishes,  be- 
yond question,  the  remarkable  character  of  the  glacial  movements 
above  indicated.  The  accompanying  diagram  (Plate  YII)  exhibits 
these  movements  to  the  eye.  The  outlines  of  the  main  rivers,  and 
the  principal  bodies  of  water,  are  indicated  by  dotted  lines.  The  rock 
ledge  that  forms-  the  eastern  margin  of  the  Green  Bay  valley  is  indi- 
cated by  a  line  of  small  crosses. 

Fiords.  In  addition  to  what  has  been  said,  the  peninsula  lying 
east  of  Green  Bay,  merits  special  consideration,  by  virtue  of  its  pe- 
culiar features.  The  Green  Bay  side  of  the  peninsula  is  high,  bold 
and  precipitous,  while  the  Lake  Michigan  shore  is  low  and  incon- 
spicuous. But  while  the  two  sides  are  in  striking  contrast  in  this  re- 
spect, they  are  conspicuously  similar  in  the  deep  indentations  that 
characterize  either  side.  And  that  which  gives  especial  interest  to 
this  is  the  correspondence  that  exists  between  them — they  are,  in 
pairs.  At  the  extreme  north  is  Hedge-hog  Harbor,  opposite  which, 
to  the  southeast,  lies  Big  Sandy  Bay,  with  a  lake  between  them.  A 
little  south  lies  Ellison's  Bay,  and  over  against  it  Rowley's  Bay.  A 
few  miles  further  south  we  find  Sister  Bay  mated  with  North  Bay. 
At  an  equal  distance  farther  south  Eagle  Harbor  stretches  far  in 
toward  Douglas'  and  Bailey's  Harbors.  Again,  Fish  Creek  and  Kan- 
garoo Lake  form  a  pair,  and  Egg  Harbor  is  linked  across  to  White 
Fish  Bay  by  lakes  and  streains,  while  Sturgeon  Bay  well  nigh  severs 
the  peninsula,  and  Little  Sturgeon  Bay  is  wedded  to  the  estuary-like 
Ahnapee  river.  Nor  is  this  a  mere  arbitrary  or  fanciful  linking.  By 
consulting  the  topographical  map  accompanying  this  report,  it  will  be 
seen  that  deep  valleys  connect  these  indentations,  and  that  a  depres- 
sion of  less  than  100  feet  would  reduce  the  peninsula  to  a  linear 


PLATE,VII 


MICHIGAN 


DIAGRAM 

Cflacial  Movements 

in 
EASTERN  WISCONSIN 

*•/ 

T.  C.  Chamberlin 
1876 


f 


QUATERNARY  FORMATIONS -THE  DRIFT.  205 

group  of  islands,  whose  counterpart  we  now  have  in  the  chain  that 
stretches  onward  to  the  north. 

Xear  North  Bay  the  surface  of  the  rock  is  beautifully  striated 
in  a  direction  varying  from  S.  1°  "W.  to  S.  13°  E.  These  striae  are 
near  the  summit  of  a  slightly  elevated  but  nearly  level  area,  and 
present  no  indications  of  local  modification.  An  inspection  of 
the  more  accurate  maps  shows  many  features  in  the  outline  of 
the  inlets  and  coast  that  harmonize  with  these  south  and  south- 
easterly groovings.  The  conclusion  is  forced  upon  the  mind  that 
the  inlets  are  glacial  troughs,  fiords,  perhaps,  we  should  call  them, 
though  they  were  not  formed  by  the  descent  of  a  glacier  from 
the  interior  of  the  peninsula  toward  the  coast  on  either  side,  but  by 
the  passage  of  the  ice  mass  across  the  peninsula,  forming  the  inden- 
tations on  the  Green  Bay  side,  in  its  ascent  of  the  ridge,  and  those 
on  the  Lake  Michigan  side  in  its  descent.  The  charts  of  the  U.  S. 
Lake  Surveys  show  that,  with  this  explanation,  the  term  fiord  is  en- 
tirely applicable.  These  troughs  are  continued  far  out  under  the 
surface  of  the  water.  On  the  Lake  Michigan  side  they  reach  from 
twelve  to  fourteen  miles  at  least  from  the  heads  of  their  respective 
bays.  At  from  eight  to  ten  miles  out  they  show  a  tendency  to  curve 
to  the  southward,  i.  e.,  to  take  a  direction  more  nearly  parallel  to  the 
axis  of  the  great  depression  in  which  the  lake  lies.  Prof.  !N".  H. 
"Winchell  has  called  attention  to  some  of  these  features,  and  has  asso- 
ciated them  in  a  very  interesting  way  with  the  general  glacial  phe- 
nomena of  the  region.1  I  was  not  aware,  however,  at  the  time  the 
fiord-like  characters  first  forced  themselves  upon  my  attention  that  he 
had  used  the  same  term  to  characterize  them. 

GLACIAL  DRIFT. 

I.  MORAINES. 

1.  Kettle  Range.  The  term  "Potash  Kettle  Eange"  has  been 
popularly  used  to  designate  an  extensive  series  of  drift  hills  and 
ridges  in  eastern  Wisconsin,  whose  full  extent  and  relationship  were 
unknown  previous  to  the  investigations  of  the  present  survey,  and 
concerning  the  true  nature  and  origin  of  which,  diverse  opinions 
have  been  held.  As  the  term  "  Potash  "  has  no  special  significance 
in  this  connection,  it  will  be  discarded.  The  northern  terminus  of 
the  range  lies  in  the  town  of  Casco,  Kewaunee  county.  From  this 

1  The  Glacial  Features  of  Green  Bay  of  Lake  Michigan,  with  some  observations  on  a 
probable  former  outlet  of  Lake  Superior.  Am.  Jour,  of  Science  and  Arts,  Vol.  II,  July, 
1871, 


206  GEOLOGY  OF  EASTERN  WISCONSIN. 

point  it  stretches  away  to  the  southwestward,  through  the  counties  of 
Manitowoc,  Sheboygan,  P'ond  du  Lac,  "Washington,  "Waukesha,  and 
into  the  northern  portion  of  Walworth.  At  this  point  it  divides,  one 
portion  extending  southward,  through  the  towns  of  Richmond  and 
Darien,  thence  eastward,  though  not  at  this  point  conspicuous,  to 
Lake  Geneva,  whence  the  main  portion  extends  northeastward  to  the 
vicinity  of  Burlington,  and  then  southward  into  Illinois.  The  other 
portion,  branching  from  the  main  range  in  the  town  of  Whitewater, 
about  twenty  miles  north  from  the  state  line,  extends  westward  to 
Hock  River,  after  crossing  which,  it  curves  gradually  to  the  north- 
ward, and  enters  the  district  examined  by  Professor  Irving,  and  will 
be  found  described  and  mapped  in  his  report  in  this  volume.  A  por- 
tion of  this  part  is  outlined  upon  the  accompanying  diagram  for  the 
convenience  of  the  reader. 

The  peculiar  feature  of  this  range  that  gives  rise  to  its  descriptive 
name,  consists  of  numerous  depressions  in  the  drift  variously  known 
as  "  Potash  Kettles,"  "  Kettles,"  "  Potholes,"  "  Pots  and  Kettles," 
" Sinks"  etc.1  Those  which  have  most  arrested  popular  attention 
are  circular  in  outline,  and  symmetrical  in  form,  not  unlike  the 
homely  utensils  that  have  given  them  a  name. 

Occasionally  they  approach  the  form  of  a  funnel,  or  of  an  inverted 
bell,  while  the  shallow  ones  are  mere  saucer-like  hollows.  But  it  is 
important  to  observe  that  large  numbers  of  these  depressions  are  not 
perfectly  circular,  but  rudely  oval,  oblong  or  elliptical,  or  are  ex- 
tended into  trough-like,  or  even  winding  hollows,  with  irregular  de- 
partures from  all  these  forms. 

In  depth,  these  depressions  vary  from  the  merest  indentation  of  the 
surface,  to  bowls  sixty  feet  or  more  deep,  while  in  the  irregular  forms 
the  descent  is  not  unfrequently  more  than  one  hundred  feet.  In  most 
of  these  cases,  however,  the  rim  is  irregular.  Symmetrical  cavities 
seldom  exceed  sixty  or  sixty-five  feet  in  depth.  The  slope  of  the  sides 
varies  greatly,  but  in  the  deeper  ones  it  very  often  reaches  an  angle 
of  30°  or  35°  with  the  horizon;  or  in  other  words,  is  about  as  steep  as 
the  material  will  lie.  In  horizontal  dimensions,  those  that  are  pop- 
ularly recognized  as  kettles  seldom  exceed  500  feet  in  diameter;  but 
considered  with  reference  to  their  origin  and  structural  nature,  they 
cannot  be  limited  to  this  dimension,  and  it  may  be  difficult  to  assign 
definite  limits  for  them.  One  of  the  peculiarities  of  the  range  is  the 
large  number  of  small  lakes  without  inlet  or  outlet  that  dot  its  course. 
So  true  is  this,  that  in  field  work  I  soon  learned  to  anticipate  the 

1  Compare,  On  the  Fresh  Water  Glacial  Drift  of  the  Northwestern  States,  by  Charles 
Whittlesey,  Smithsonian  Contributions  to  Knowledge.  1866. 


QUATERNARY  FORMATIONS  -THE  DRIFT.  207 

position  of  the  Range  from  the  distribution  of  these  lakes  on  the  map. 
Some  of  these  are  merely  ponds  of  water  at  the  bottom  of  typical 
kettles,  and  from  this  they  graduate  by  imperceptible  degrees  into 
lakes  of  two  or  three  miles  in  diameter.  These  are  simply  kettles  on 
a  large  scale. 

Next  to  the  kettles  themselves,  the  most  striking  feature  of  this 
peculiar  formation  is  their  counterpart  in  the  form  of  rounded  hills 
and  hillocks,  which  may  not  inaptly  be  called  inverted  kettles.  These 
give  to  the  surface  an  irregularity  sometimes  designated,  not  inap- 
propriately, as  knobby  drift.  The  trough-like,  winding  depressions 
have  their  counterpart  in  sharp,  serpentine  ridges.  The  combined 
effect  of  these  elevations  and  depressions  is  to  give  to  the  surface  an 
entirely  distinctive  character. 

These  features,  however,  may  be  regarded  as  subordinate  elements 
of  the  main  range,  since  these  hillocks  and  depressions  are  variously 
distributed  over  its  surface.  They  are  usually  most  abundant  upon 
the  more  abrupt  face  of  the  range,  but  occur  in  greater  or  less  degree 
on  all  sides  of  it,  and  in  various  situations.  Not  infrequently  they 
occur  extensively  distributed  over  comparatively  level  areas  adjacent 
to  the  range.  Sometimes  they  prevail  in  the  valleys,  the  adjacent  hills 
being  free  from  them;  and  again  they  are  present  upon  the  hills, 
but  are  wanting  in  the  adjacent  valleys.  These  facts  have  an  import- 
ant bearing  in  considering  the  question  of  their  origin,  which  may 
best  be  deferred  until  all  the  facts  are  presented.  The  range  itself  is 
of  composite  character,  being  made  up  of  a  series  of  essentially  par- 
allel drift  ridges  that  unite,  interlock,  separate,  appear  and  disappear 
in  an  irregular  and  intricate  manner.  At  least  four  of  these  subordi- 
nate ridges  are  often  clearly  discernible,  and  at  points  the  number  is 
considerably  increased.  Associated  with  the  main  range,  there  are 
occasionally  sharp  gravel  ridges,  known  as  "hog's-backs,"  rising  as 
abruptly  as  the  nature  of  the  material  will  admit,  to  the  height  of  20 
or  30  feet,  and  occasionally  to  60  feet,  or  even  more.  These  usually 
lie  upon  the  flanks  of  the  more  massive  ridges,  and  are  distinguished 
from  the  serpentine  ridges  spoken  of  before  in  no  essential  way  except 
in  their  greater  size,  extent  and  distinctness.  It  is  usually  between 
the  parallel  ridges,  and  occupying  depressions  evidently  caused  by 
their  divergence,  that  most  of  the  larger  lakes  associated  with  the 
range  are  found.  Ridges  running  across  the  general  trend  of  the 

o  Cj  O  o 

range,  as  well  as  transverse  spurs  extending  out  from  it,  are  not  un- 
common features.  The  component  ridges  are  themselves  exceedingly 
irregular  in  height  and  breath,  being  often  much  broken  and  inter- 
rupted. The  combined  effect  of  all  the  foregoing  features  is  to  give 


208  GEOLOGY  OF  EASTERN  WISCONSIN. 

to  the  formation  an  exceedingly  irregular  and  complicated  aspect. 
It  is  apparently  the  equivalent  of  the  Kames  of  Scotland,  and  Prof. 
Geikie's  graphic  description  is  specifically  applicable  to  our  Kettle 
Range : 

"The  sands  and  gravels  have,  as  I  have  just  said,  a  tendency  to  shape  themselves 
into  mounds  and  winding  ridges,  which  give  a  hummocky  and  rapidly  undulating  out- 
line to  the  ground.  Indeed,  so  characteristic  is  this  appearance,  that  by  it  alone  we  are 
often  able  to  mark  out  the  boundaries  of  the  deposit  with  as  much  precision  as  we  could 
were  all  the  vegetation  and  soil  stripped  away  and  the  various  subsoils  laid  bare.  Oc- 
casionally, ridges  may  be  tracked  continuously  for  several  miles,  running  like  great 
artificial  ramparts  across  the  countiy.  These  vary  in  breadth  and  height,  some  of  the 
more  conspicuous  ones  being  upwards  of  four  or  five  hundred  feet  broad  at  the  base,  and 
sloping  upwards  at  an  angle  of  25°  or  even  35°  to  a  height  of  60  feet  and  more,  above 
the  general  surface  of  the  ground.  It  is  most  common,  however,  to  find  mounds  and 
ridges  confusedly  intermingled,  crossing  and  recrossing  each  other  at  all  angles,  so  as 
to  enclose  deep  hollows  and  pits  between.  Seen  from  some  dominant  point,  such  an 
assemblage  of  kames,  as  they  are  called,  looks  like  a  tumbled  s.ea  —  the  ground  now 
swelling  into  long  undulations,  now  rising  suddenly  into  beautiful  peaks  and  cones,  and 
anon  curving  up  in  sharp  ridges  that  often  wheel  suddenly  round  so  as  to  enclose  a  lake- 
let of  bright,  clear  water." 

The  width  of  the  Range  is  from  one  to  ten  miles,  and  its  peaks  oc- 
casionally rise  300  feet  above  its  base. 

Gravel,  sand,  bowlders  and  clay  constitute  the  material  of  the  Range, 
and  are  variously  intermingled  in  its  composition.  On  the  whole, 
gravel  is  the  most  prominent  element  exposed  to  observation.  It  is 
usually  coarse  but  very  irregular,  and  frequently  full  of  rounded 
bowlders.  It  is  to  be  noticed  that  the  cobble  stones  are  spherically 
rounded  and  not  flat,  as  is  common  in  the  beach  gravel  along  Lake 
Michigan.  They  are  chiefly  composed  of  the  magnesian  limestone  of 
the  region.  The  sand  is  usually  associated  with  the  gravel,  and  it  is 
only  occasionally  that  a  deposit  of  pure  sand,  free  from  gravel  or 
bowlders,  is  found.  The  clay  is  usually  of  a  light  color,  moderately 
tough,  calcareous  in  composition,  and  contains  imbedded  in  it  erratics 
of  all  sizes  from  those  more  than  ten  feet  in  maximum  diameter  down 
to  pebbles.  Bowlders  of  Archaean  rock  are  subordinate  in  numbers 
to  those  of  the  Paleozoic  formations,  except  where  clustered  in  partic- 
ular localities,  as  occasionally  happens.  But  from  the  fact  that  no 
Archaean  formation  is  known  to  exist  near  the  Range,  the  special  dis- 
tribution of  this  class  of  bowlders  is  of  little  importance.  Quite  the 
contrary,  however,  with  the  limestone  erratics,  which  are  especially 
demonstrative  of  its  origin  and  formation. 

Near  Burlington  there  is  an  exposure  of  a  thin-bedded,  rather 
argillaceous  dolomite,  different  from  any  seen  elsewhere,  and  contain- 
ing the  Trilobite,  lllcenus  im/perator,  in  considerable  numbers,  with 


QUATERNARY  FORMATIONS  —  THE  DRIFT. 


209 


but  few  other  fossils.  Nothing  that  could  be  mistaken  for  it  by  a 
careful  observer  has  yet  been  found  elsewhere  in  the  state.  In  the 
Kettle  Range,  southwest  of  Burlington,  large  quantities  of  this  rock 
are  found,  and  at  heights  very  considerably  above  the  present  surface 
of  the  rock.  The  blocks  are  usually  somewhat  worn,  but  still  sub- 
angular.  Their  identity  is  put  beyond  question  by  the  presence  of 
Illcenus  imperator. 

Passing  northward  along  the  Eange,  in  the  town  of  Whitewater, 
there  appear  large  masses  of  the  subjacent  Galena  limestone,  distrib- 
uted upon  and  through  the  drift,  being  found  at  from  150  to  175  feet 
above  the  bed  rock  in  the  vicinity.  These  erratics  are  frequently 
very  little  worn,  and  in  one  case  a  stratified  mass  that  seemed  to  have 
been  bodily  transported  was  found  at  least  100  feet  above  the  bed 
rock.  Metamorphic  and  igneous  erratics  occur  in  great  abundance 
and  variety  here. 


Section  cf  the  Kettle  Eange  on  the  line  of  the  C.,  P.  &  L.  S,  R.  R.,  southeast  of  Whitewater.  The 
figures  show  the  elevation  above  Lake  Michigan.  The  north  ridge  is  composed  of  exceedingly 
coarse,  mixed  material. 

In  the  towns  of  Palmyra  and  Eagle  where  the  Kange  crosses  the 
Cincinnati  group,  large  quantities  of  the  peculiar  areno-argillaceous 
and  calcareous  shales,  belonging  to  the  lower  portion  of  that  forma- 
tion, and  which  on  the  east  side  of  Lake  Wmnebago  lie  at  from  175 
to  200  feet  below  the  upper  face  of  the  group,  are  found  in  the  ridges 
of  the  Range.  It  is  a  soft  rock  that  could  not  resist  much  abrasive 
action,  and  yet  it  predominates  in  some  of  the  ridges  over  all  other 
forms.  It  contains  an  abundance  of  small  linguloid  fossils,  rendering 
its  identification  beyond  question.  Although  so  abundant  here,  these 
bowlders  are  found  but  very  rarely  except  for  six  or  eight  miles  along 
the  Range  where  it  crosses  the  formation  from  which  they  were  evi- 
dently derived.  They  are  most  abundant  in  the  ridges  on  the  west 

side  of  the  Range. 

FIG.  6. 


Profile  across  the  Kettle  Range  from  Eagle  westward. 

SUE.  — 14 


210  GEOLOGY  OF  EASTERN  WISCONSIN. 

In  the  same  region,  bowlders  of  clay,  which  probably  originated 
in  the  argillaceous  layers  of  the  Cincinnati  group,  occur,  imbedded 
in  the  common  drift  mass. 

Immediately  beyond  this,  in  the  northern  part  of  Eagle,  and  on- 
ward, where  the  range  passes  over  the  thick,  heavy  beds  of  the  Niag- 
ara Group,  the  drift  is  characterized  by  great  blocks  of  that  forma- 
tion, often  but  little  eroded.  Here,  as  well  as  southward,  there  is 
present  a  very  considerable  portion  of  well-worn,  white,  compact, 
fine-grained,  often  cherty,  dolomite,  that  probably  came  from  the 
"Waukesha  beds  of  the  Niagara  Group,  on  the  east  side  of  the  Range. 
"When  we  reach  the  central  and  northern  parts  of  Washington 
county,  large  quantities  of  dolomitic  sand  enter  into  the  composition 
of  the  drift.  This  is  especially  true  'of  the  eastern  flank.  The  sand 
arises  unquestionably  from  the  crushing  of  the  granular  dolomites  of 
the  Racine  limestone,  which  is  the  prevailing  rock  to  the  east  and 
which  underlies  the  Range  in  part  in  this  region.  The  northern  and 
southern  limits  of  this  sand  are  very  nearly  coincident  with  the 
northern  and  southern  limits  of  the  granular  rock  in  the  vicinity  of 
the  Range. 

Large  bowlders  of  brecciated  limestone,  containing  Pentamerus  ob- 
longus,  are  found  in  this  region,  and  on  the  west  side  of  the  Range  in 
the  towns  of  Kewaskurn,  Ashford  and  Auburn,  beds  crowded  with 
this  fossil  are  found  in  situ. 

In  the  northern  part  of  Sheboygan  and  the  southern  part  of  Mani- 
towoc  counties,  blocks  from  the  Upper  Coral  and  Racine  beds,  along 
which  the  ridge  runs,  form  the  most  marked  constituent  of  the  drift, 
and  similar  facts  are  true  to  the  extremity  of  the  Range. 

It  appears  then  that  throughout  its  extent,  the  neighboring  or  un- 
derlying rock  has  contributed  a  noticeable  element  to  the  composition 
of  the  Range.  To  this  extent  its  local  origin  is  clearly  demonstrated. 
At  the  same  time  it  is  an  equally  conspicuous  fact  that  there  is  pres- 
ent at  all  points  a  large  percentage  of  material  which  had  a  more  re- 
mote origin.  It  is  not  difficult  at  a  single  point  to  find  specimens 
representing  several  of  the  formations  of  this  state  besides  those  of 
Michigan.  Native  Copper  is  found  quite  frequently  at  all  points 
along  the  Range,  and  must  have  traveled  from  one  to  three  hundred 
miles.  It  is  evident  then  that  the  agency  which  produced  the  Range, 
gathered  its  material  all  along  its  course  for  at  least  three  hundred 
to  the  northward,  and  that  its  largest  accumulations  were  in 
immediate  vicinity  of  the  deposit. 

. — The  formation  presents  both  the  stratified  and  un- 
condition.     If  we  could  trust  to  such  exposures  as  wj  s  e 


QUATERNARY  FORMATIONS  -  THE  DRIFT. 


211 


along  highways  and  streams,  the  stratified  condition  would  unques- 
tionably be  considered  the  prevailing  L-rm  of  structure,  but  these  are 
very  often  deceptive.  The  flanks  of  all  drift  ridges  become  stratified 
by  wash,  winds  and  gravitation,  whether  originally  so  or  not,  and  the 
excavation  of  a  road  or  stream  is  much  more  apt  to  expose  this  por- 
tion than  the  real  nucleus  of  the  hill.  The  deeper  excavations  that 
have  been  made,  however,  demonstrate  that  to  a  large  extent,  at  least, 
the  core  of  the  Range  is  unstratified. 

A  few  additional  features  deserve  consideration,  among  which  is 
the  comparative  abruptness  of  the  opposite  slopes  of  the  Range.  In 
treating  of  this  and  the  following  topics,  reference  will  be  had  chiefly 
to  the  eastern  and  main  portion  of  the  Range,  since  the  recurving 
western  branch  is  not  sufficiently  conspicuous  to  render  observations 
of  this  kind  of  special  value. 

In  the  town  of  Randall,  Kenosha  county,  the  eastern  face  is  quite 
abrupt.  Between  Burlington  and  Lake  Geneva,  the  more  abrupt  face  is 
toward  the  northwest.  The  same  is  true  in  the  towns  of  Richmond, 
Whitewater,  La  Grange,  Palmyra,  Eagle,  Ottawa,  and  Delafield.  In 
Washington  county  the  difference  in  the  abruptness  of  the  two  sides 
is  less  marked,  but  the  general  truth  is  the  same.  Likewise  in  She- 
boygan  county,  in  general.  In  the  towns  of  Plymouth  and  Rhine,  the 
eastern  face  is  well  defined,  but  the  fine  development  of  kettles,  men- 
tioned and  figured  by  Col.  Whittlesey,  occurring  near  Greenbush,  lie 
upon  the  northwestern  flank,  and  the  western  face  in  the  town  or 
Rhine  is  also  sharply  limited,  and  the  peculiar  features  of  the  Range 
are  more  strongly  marked  on  this  than  upon  the  opposite  side.  In 
Manitowoc  and  Kewaunee  counties  both  flanks  as  well  as  the  whole 
Range  are  much  subdued  and  neither  presents  sharp  outlines. 

It  is  a  general  and,  indeed,  a  pretty  well  sustained  fact  that  the 
westward  face  of  the  Range  is  the  more  abrupt,  and  that  the  more 
conspicuous  peculiarities  of  the  formation  lie  upon  that  side.  Long, 
sharp  ridges,  termed  hog's  backs,  occur  in  Wai  worth  and  Waukesha 
counties,  flanking  the  main  ridge,  but  have  no  counterpart  upon  the 
east  side  of  the  Range. 

FIG.  7. 


Profile  across  the  west  branch  of  the  Kettle  liauge  south  of  Whitewater,  showing  the  position  of 
the  "kettles"  on  the  northern  slope. 


212  GEOLOGY  OF  EASTERN  WISCONSIN. 

The  general  relationship  of  this  Ilange  to  the  rock  terrane  that  un- 
derlies it  has  already  been  stated  under  the  head  of  Topography,  viz. : 
that  the  southern  portion  rests  upon  its  crest,  and  the  northern  upon 
its  eastern  slope.  Instead  of  lying  along  the  ridgepole  of  this  rocky, 
one-sided  roof,  the  northern  end  has  slid  half  way  down  to  the  eaves. 
But  something  more  of  detail  as  to  its  topographical  relations  is 
needed. 

Beginning  again  in  the  town  of  Randall,  its  abrupt  face  looks  out 
eastward  upon  a  comparatively  level  surface  with  no  intervening  land 
of  equal  height  between  it  and  the  lake.  The  opposite  side  in  the 
town  of  Walworth  is  also  higher  than  the  surface  west  of  it.  The 

o 

.Range  between  Burlington  and  Geneva  faces  higher  land  on  the  oppo- 
site side  of  the  White  river.  In  the  northwestern  part  of  Walworth 
county  there  is  a  broad  area  of  much  lower  land  to  the  northwest, 
while  on  the  opposite  side  of  the  Range  the  surface  rises  toward  Elk- 
horn,  which  is  the  highest  portion  of  the  county.  The  surface  in 
Mukwonago  rises  higher  than  that  of  the  Range  in  Eagle,  and  in  Wau- 
kesha  county  generally,  the  surface  is  higher  to  the  east  than  the  base 
of  the  Range,  although  its  peaks  are  the  highest  points  in  the  county. 
Throughout  Washington  county,  except  along  the  northern  line,  the 
ridge  is  conspicuously  higher  than  the  surface  on  either  hand.  In 
Sheboygan  and  Fond  du  Lac  counties,  it  is  much  higher  than  the  sur- 
face east,  but  barely  equals  the  highlands  of  Taycheedah,  Empire  and 
Eden  on  the  west.  Beyond  this  it  is  higher  than  the  surface  east, 
but  lower  or  barely  equal  to  that  west. 

It  should  be  borne  in  mind  that  these  comparisons  have  reference 
to  the  summit  of  the  Range,  and  that  the  base  may  be  reckoned  200 
feet  lower  on  the  average.  This  fact  is  the  more  important,  since  in 
considering  the  question  of  its  origin,  the  elevation  of  the  base  and 
not  of  the  summit  is  the  important  consideration. 

Taking  this  into  account,  it  becomes  a  conspicuous  fact  that, 
setting  aside  the  irregularities  near  the  state  line,  the  Kettle  Range 
in  the  southern  portion  is  flanked  on  the  east  by  higher  lands,  that 
near  the  center  it  attains  the  supremacy,  and  that  in  the  northern  por- 
tion it  is  overtopped  by  highlands  on.  the  west. 

This  is  not  to  be  considered  as  at  variance  with  the  statement 
already  made  in  reference  to  the  rock  ridge  that  underlies  it,  for  the 
highlands  to  the  east  of  it  in  the  southern  portion  are  great  drift 
hills,  but  of  regular,  rounded  contour  as  previously  described. 

And  I  may  here  again  call  attention  to  the  fact  that  the  hills  and 
ridges  on  the  east  of  the  range  have  an  east-west  trend,  and  those  on  the 
opposite  side,  a  north-south  trend,  or  unessential  variations  from  these. 


QUATERNARY  FORMATIONS —  THE  DRIFT,  213 

All  these  facts,  which  have  been  matters  of  careful  attention,  are 
of  supreme  importance  in  considering  the  origin  of  this  remarkable 
formation. 

The  summit  altitudes  of  a  few  of  the  more  prominent  points  will 
be  of  interest  in  this  connection.  Others,  if  desired,  may  be  found  in 
the  list  of  elevations  previously  given,  or,  in  a  general  way,  by  refer- 
ence to  the  topographical  map. 

In  Sec.  36,  S.  hf.,  S.  E.  qr.,  Randall,  near  the  state  line 340  feet. 

Near  the  state  line  in  the  towns  of  Linn  and  Wai  worth,  above 400    " 

The  observations  not  being  sufficiently  reliable  to  warrant  a  more 

exact  statement. 

Tree  Bluff,  Sec.  24,  near  center,  Whitewater  . . . '. 457 

Bald  Bluff,  Sec.  33,  S.  E.  qr.,  Palmyra 463 

Government  Hill,  town  of  Delafield 611 

Lapham's  Peak,  Sec.  14,  Erin 824 

Sugar  Loaf  in  Sec.  24,  near  middle  S.  line,  Hartford 740 

Hill  near  middle  S.  line,  Sec.  2,  Mitchell 580 

Top  of  Range,  N.  W.  qr.,  Sec.  5,  Memee 348 

Last  prominent  hill  in  the  Range  at  the  north,  middle  W.  hf.,  Sec.  13, 

Casco  235 


The  Range  then  reaches  its  culmination  in  Lapham's  Peak,  824 
feet  above  Lake  Michigan.  Several  of  these  hills  rise  from  150  feet 
to  250  feet  above  their  immediate  bases.  The  depth  of  the  drift  can- 
not be  less  than  300  feet  at  many  points  along  the  ridge,  from  which 
we  see  that  the  accumulation  is  vast,  and  that  the  force  that  heaped  it 
up  must  have  been  powerful. 

The  foregoing  facts  gather  themselves  into  a  mass  of  evidence 
whose  force  is  altogether  irresistible.  The  Kettle  Range  is  evidently 
a  gigantic  moraine.  The  main  Range  from  Kewatinee  county  to 
Walworth  county  marks  the  westward  limit  of  the  glacier  that  oc- 
cupied the  basin  of  Lake  Michigan,  and  the  eastern  limit  of  the  one 
that  plowed  through  the  Green  Bay  valley.  The  branch  that  extends 
southward  into  Illinois,  is  the  continuation  of  the  terminal  moraine 
of  the  Lake  Michigan  glacier.  The  branch  that  recurves  through  the 
northern  part  of  Rock  county  and  thence  northward,  is  the  terminal 
moraine  of  the  Green  Bay  glacier,  upon  that  side. 

Keither  of  these  indicates  the  extreme  limits  of  the  glacial  move- 
ment, for  in  the  eastern  part  of  Rock  county,  although  striae  are 
absent,  the  contour  of  the  hills,  together  with  the  composition  of  the 
drift,  show  that  the  movement  was  from  the  eastward.  In  the  vicinity 
of  Beloit,  fossils  of  the  Racine  limestone  are  common.  On  the  other 
hand,  the  train  of  bowlders  extending  southwestward  from  the 


214:  GEOLOGY  OF  EASTERN  WISCONSIN. 

quartzite  in  the  towns  of  Portland  and  "Waterloo,  stretches  directly 
across  the  Range  and  onward  into  Illinois.  It  seems  evident,  then, 
that  before  the  formation  of  the  Kettle  Range,  the  glacial  movements 
were  essentially  the  same  as  they  were  subsequent  to  its  formation, 
and  that  its  accumulation  was  due  to  unusual  conditions  afi'ecting  the 
rate  of  the  recession  of  the  glaciers.  The  structure  of  the  Range 
seems  to  indicate  an  alternating  retreat  and  advance  of  the  ice-mass. 
During  the  former,  debris  was  thrust  out  at  the  foot  of  the  melting 
mass,  which,  when  the  glacier  advanced,  was  plowed  up  into  im- 
mense ridges. 

If  this  process  be  supposed  to  be  repeated  several  times,  parallel 
ranges  will  be  accounted  far,  and  the  irregularities  incident  to  such 
retreat  and  advance  will  explain  the  complexity  of  the  Range.  Where 
the  later  advances  were  equal  to  the  earlier  ones,  the  whole  accumula- 
tion of  drift  material  would  be  forced  into  a  single  massive  ridge. 
Where  any  advance  failed  to  equal  a  former  one,  an  interval  between 
the  accumulations  of  the  two  would  result,  giving  rise  to  a  depression 
whose  form  would  depend  upon  the  relations  of  the  two  accumula- 
tions, but  would,  in  general,  be  more  or  less  trough-like  in  character. 
Where  tongues  of  ice  were  thrust  into  the  accumulated  material,  a 
serrated  edge  or  projecting  spurs  and  corresponding  indentures  would 
result.  If  masses  of  the  ice  became  incorporated  within  the  drift,  as 
has  been  suggested,  their  subsequent  melting  would  give  rise  to  a  de- 
pression constituting  one  form  of  the  kettles  which  characterize  the 
range.  The  suggestion  just  made,  with  reference  to  the  irregular  ad- 
vance of  the  ice  mass,  accounts  for  other  forms,  and  at  the  same  time 
for  the  irregular  hills,  mounds  and  ridges  that  are  so  conspicuous  a 
feature  of  the  Range. 

Certain  of  the  "kettles  "  may  have  an  origin  diverse  from  either  of 
the  causes  above  suggested.  A  portion  of  the  material  of  the  forma- 
tion is  a  loose  quicksand,  easily  removed  by  the  action  of  water.  The 
irregular  surface  of  the  Range,  and  its  porous  character,  facilitate  the 
collection  of  water,  which  issues  from  its  base  in  numerous  perennial 
springs;  indeed,  in  some  cases,  brooks  of  no  inconsiderable  size  flow 
full-fledged  from  its  base.  These  are  entirely  competent  to  carry 
away,  through  their  underground  channels,  quicksand  and  similar 
material,  thus  undermining  the  surface  and  causing  a  depression.  It 
may  be  prudent  to  remark  in  this  connection,  that  depressions  alto- 
gether similar  to  many  of  those  under  consideration  occur  within 
eastern  Wisconsin,  which  are  manifestly  due  to  very  different  causes. 
One  of  these  is  the  well  known  formation  of  sink-holes  in  limestone 
districts,  by  the  dissolving  out  and  removal  of  the  rocks  by  under- 


QUATERNARY  FORMATIONS  —  THE  DRIFT. 


215 


giound  drainage.  Of  similar  nature  to  these  are  those  cases  in  which 
the  drift,  by  its  open  nature,  furnishes  underground  channels  of 
drainage.  A  marked  instance  of  this  kind  occurs  in  the  vicinity  of 
Beloit.  During  the  spring  of  187G  and  1877,  a  very  considerable 
stream  flowed  for  several  weeks  into  a  shallow  basin,  and  was  entirely 
lost.  Another  class,  but  of  insignificant  importance,  is  due  to  the  ac- 
tion of  lakes,  in  throwing  up  ridges  across  small  bays  or  indentures 
along  their  shores.  These,  however,  are  rarely  so  symmetrical  as  to  be 
misleading,  and  their  situation  is  such  as  to  readily  indicate  their  origin. 

In  the  vicinity  of  the  Kettle  Range  proper,  and  at  several  localities 
more  or  less  distant  from  it,  there  are  areas  presenting  a  similar  un- 
dulating surface,  marked  by  the  peculiar  hills  and  basins  that  charac- 
terize that  formation.  These  unquestionably  owe  their  origin  to  a 
similar  cause,  save  that  it  was  local  and  circumscribed  in  character. 
Owing  to  their  limited  extent  and  general  inconspicuous  character, 
they  do  not  require  extended  or  special  description  in  this  connection. 
One  of  the  best  examples  of  this  class  is  to  be  found  in  the  vicinity 
of  Rock  Lake,  in  Jefferson  county. 

2.  Minor  Moraines.  It  will  be  most  convenient  to  consider  in 
this  connection  certain  minor  morainic  features  of  no  very  great  ex- 
tent or  importance  in  themselves,  except  from  their  interesting  char- 
acter. The  most  noteworthy  of  these  occurs  in  sections  4,  5  and  6  of 
the  town  of  Herman,  and  in  sections  33  and  34  in  the  town  of  Theresa, 
Dodge  county.  It  consists  of  a  narrow,  well  defined  ridge,  rising  not 
usually  more  than  twenty  feet  in  height,  extending  in  a  general  east- 
erly and  westerly  direction  for  a  distance  of  about  three  miles,  with 
occasional  interruptions  where  it  is  crossed  by  streams  and  dry  runs. 
The  accompanying  rude  map  shows  its  topographical  character  and 
relations.  At  its  western  extremity  it  is  terminated  by  a  remarkable 
transverse  ridge,  oblique  to  the  main  range,  as  is  imperfectly  repre- 
sented on  the  map. 

FIG.  8. 


Map  of  Moraine  In  the  towns  of  Herman  and  Theresa. 


216  GEOLOGY  OF  EASTERN  WISCONSIN. 

2sear  the  western  extremity,  there  is  a  conspicuous  north  and  south 
drift  range,  over  which  the  minor  ridge  under  consideration  passes; 
and  in  doing  so,  it  curves  to  the  northward  in  a  very  peculiar  manner. 
Throughout  sections  5  and  6,  the  ridge  lies  upon  an  elevated  table- 
land or  plateau  formed  of  drift  material.  To  the  east  of  this  it  grad- 
ually curves  to  the  northeastward  and  descends  to  a  considerably 
lower  level,  the  eastern  extremity  being  very  much  lower  than  the 
western.  The  two  peculiarities  worthy  of  special  notice  are  the  fact 
that  it  is  a  drift  ridge,  superposed  upon  an  evidently  earlier  drift  for- 
mation, to  whose  surface  configuration  it  conforms  in  a  measure,  and 
the  fact  that  its  elevation  is  markedly  different  in  different  portions. 
These  facts  are  sufficient  to  show  of  themselves  that  it  could  not  be 
formed  by  the  action  of  water,  since  no  supposable  warping  of  the 
.earth  could  bring  it  into  such  a  position  as  to  constitute  the  margin  of 
a  lake  or  other  body  of  water  supposed  to  be  capable  of  forming  such 
a  ridge,  and  for  the  same  reason  its  origin  cannot  be  attributed  to 
floating  ice.  In  addition  to  these  facts,  its  structure  and  the  material 
of  which  it  is  composed,  forbid  such  a  supposition.  It  is  composed 
of  confusedly  intermingled  coarse  and  fine  unstratified  material.  A 
large  number  of  bowlders  of  various  classes  of  rocks  —  Paleozoic  and 
Archaean  — are  imbedded  in  sand,  gravel,  and  clay,  in  most  promiscu 
ous  confusion,  and  in  sonie  cases  in  such  a  position  as  would  forbid 
the  supposition  that  they  were  deposited  upon  the  surface  of  a  grad- 
ually accumulating  mass.  In  one 
"Fio  9 

instance  a  mass  of  finely  laminated 

clay,  apparently  a  clay  bowlder, 
was  found  surrounded  by  the  com- 
mingled unstratified  material.  The 
accompanying  figure  illustrates  the 

SECTION  OF  MORAINE  IN  TOWN  OF  HERMAN.      general   nature   of    the    structure   of 

the  ridge.  It  is  apparently  due  to  a  local  advance  of  the  thinned 
edge  of  the  glacier  upon  the  surface  of  drift  already  deposited,  roll- 
ing up  the  ridge  in  front  of  it.  It  will  be  evident  that  such  an  ad- 
vance would  be  retarded  by  the  north  and  south  ridge  in  section  6,  if 
the  thickness  of  ice  were  inconsiderable,  and  at  the  same  time  its 
melting  hastened,  which  accounts  for  the  peculiar  flexure  of  the  mo- 
raine in  crossing  it. 

A  similar  chain  of  hills  and  ridges  occurs  in  sections  16,  21  and  27 
in  the  town  of  Beloit.  The  base  of  the  chain  at  its  eastern  extremity 
has  an  elevation  of  about  200  feet  above  Lake  Michigan.  As  it  ex- 
tends northwestward,  the  surface  upon  which  it  rests  rises  until  the 
moraine  rests  upon  the  crest  of  a  rock  ridge,  at  least  250  feet  in 


QUATERNARY  FORMATIONS  —  THE  DRIFT. 


217 


elevation,  over  which  it  passes  obliquely  and  descends  into   a  pre- 
glacial  valley.      The  material  of  this  chain  is  chiefly  composed  of 
rounded,  well-wTorn  limestone  gravel,  mingled  with  a  large  propor- 
FIG.  10.  tion  of  sand,  and  more  or  less  clay, 

with  occcasional  small  bowlders,  as 
in  the  preceding  case.  !Nb  flexure 
of  the  crust  can  be  supposed  to 
have  taken  place,  capable  of  bring- 
ing the  bases  of  these  hills  and 
ridges  to  the  same  level,  which 
would  be  necessary  in  accounting 
for  them  by  the  action  of  water  or 
floating  ice.  Besides,  the  general 
configuration  of  the  adjacent  coun- 
try and  the  nature  of  its  superficial 
deposits  preclude  the  idea  of  sub- 
mergence of  either  side  of  the  range. 
Another  case  occurs  in  the  valley 
of  Grand  river,  between  the  vil- 
lage of  Markesan  and  Manchester, 
in  Green  Lake  county.  The  chain 
of  drift  hills  stretches  across  the 
main  valley,  which  is  occupied  by 
the  Grand  river,  and  was  doubtless  originally  the  cause  of  the  detour 
which  that  stream  makes  through  the  site  of  the  village  of  Markesan. 
In  all  of  the  three  cases  above  mentioned,  the  general  direction  of  the 
ridges  is  transverse  to  that  of  glacial  movement,  which  harmonizes 
with  the  view  here  entertained,  that  they  are  terminal  moraines. 

II.  BOWLDER  CLAY,  OR  TILL., 

Reference  has  already  been  made  to  the  fact,  that,  previous  to  the 
formation  of  the  great  moraine,  the  Kettle  Range,  the  glacier  pushed 
southward  in  the  Rock  river  valley,  abrading  the  surface,  modifying 
its  contour,  and  finally,  on  its  retiring,  left  the  material  strewn  upon 
the  surface.  This  constitutes  the  earliest  drift  formation  within  the 
limits  of  the  dis'":  '"t  under  consideration.  It  consists  of  a  commingled 
mass  of  clay,  sand,  gravel,  and  bowlders  variously  arranged  with  ref- 
erence to  each  other,  and  spread  out  irregularly  over  the  surface  of 
the  rock  below.  As  would  naturally  occur  under  the  circumstances, 
a  portion  of  this  is  sorted  and  stratified,  forming  beds  of  brick  clay 
or  of  sand  or  of  gravel,  and  leaving  in  certain  localities  accumulations 


Moraine  in  the  town  of  Beloit. 


218  GEOLOGY  OF  EASTERN  WISCONSIN. 

of  coarser  material.  This  action  took  place  in  part  simultaneously  with 
the  formation  of  the  deposit,  and  so  these  rearranged  and  stratified 
beds,  mingle  irregularly  with  the  unsorted  material.  Taken  as  a  class, 
this  constitutes  the  original  glacial  deposit  or  ground  moraine,  and 
in  this  report  it  is  known  by  its  most  characteristic  feature,  Bowlder 
Clay,  or  by  the  term  Till.1  That  portion  of  the  bowlder  clay  which 
antedates  the  formation  of  the  Kettle  Range  merges  into  that  forma- 
tion, and  on  the  opposite  side,  a  precisely  similar  deposit  of  bowlder 
clay  takes  its  origin  from  the  great  moraine  and  spreads  over  the  re- 
maining area  of  the  district,  although  overlaid  in  part  by  subsequent 
formations.  So  it  appears  that  the  Kettle  moraine  is  simply  a  pecu- 
liar and  irregular  aggregation  of  this  wide-spread  ground  moraine. 
In  relative  age  then,  a  portion  of  the  Bowlder  Clay  is  older  than  the 
Kettle  Range,  and  a  portion,  more  recent,  there  being  no  essential  dis- 
tinction in  character  between  the  two  parts. 

If  we  descend  to  a  more  special  and  critical  examination  of  the 
material  of  this  formation,  the  clay,  the  chief  element,  will  be  found 
to  be  of  the  most  heterogeneous  character.  The  prevailing  color  i  s 
blue,  but  it  is  not  unfrequently  reddish,  greenish,  earthy  brown,  or 
ashy.  In  texture,  it  varies  from  that  which  is  highly  plastic  and  ad- 
hesive to  varieties  so  arenaceous  and  friable  as  scarcely  to  cohere  in 
lumps.  In  general,  however,  it  is  intermediate  between  these  ex- 
tremes, being  marly  in  character.  The  imbeded  bowlders  are  of  all 
sizes  from  those  that  weigh  many  tons  downwards,  and  are  as  various 
in  character.  A  large  proportion  of  those  at  any  given  point  are 
usually  from  the  subjacent  rock,  or  from  some  formation  in  the  im- 
mediate vicinity,  but  there  is  usually  present,  a  large  proportion  of 
Archaean  erratics.  Along  the  lake  shore  there  are  many  bowlders  that 
represent  various  formations  newer  than  any  known  to  exist  in  Wis- 
consin, having  doubtless  been  derived  from  the  basin  of  the  lake,  or 
from  Michigan. 

These  bowlders  show  every  degree  of  erosion.  Some  have  not  only 
been  thoroughly  rounded  but  have  suffered  much  reduction  in  size, 
as  is  shown  by  the  projection  of  the  harder  and  more  unyielding  por- 
tions, giving  the  specimen  often  a  unique  and  fanciful  form.  Some 
specimens  are  polished  and  striated  on  one  side,  but  rough  and  an- 
gular on  the  others,  due  doubtless  to  their  having  been  firmly  im- 
bedded in  the  under  surface  of  the  glacier,  and  so  polished  as  they  were 
forced  along  over  the  rocky  surface  below.  Other  fragments  are  al- 
most wholly  unmodified,  though  often  of  soft  and  fragile  material. 

1  See  The  Great  Ice  Age,  by  James  Geikie,  1874. 


'>  I  U  U  A  It  V 

L'XIVKKsiTV   of 

CALIFORX!  A 


I 


5  I  g  a  s 


PLATE,VIII 


! 


s 


ik 


FIG.  11. 


QUATERNARY  FORMATIONS  —  THE  DRIFT. 

Usually  such  specimens  have  been  derived  from  the  immediate  vicin- 
ity, but  such  does  not  seem  to  be  always  the  case. 

An  interesting  peculiarity, 
sometimes  observed,  consists  of 
cavities  filled  with  fine  uniform 
gravel,  which  presents  the  appear 
ance  of  having  been  deposited  in 
the  form  of  gravel  bowlders,  either 
cemented,  or,  as  suggested  by  Dr. 
E.  Andrews,  in  the  frozen  state. 
These  have  been  observed  of  va- 
rious sizes,  from  six  inches  to  two 
or  three  feet  in  diameter,  and  of 
irregular,  though  usually  some- 
what rounded,  forms,  as  shown  in 
the  accompanying  figure. 

This  figure  also  imperfectly  il- 
lustrates the  irregular  stratifica- 
tion and  lamination  which  fre- 
quently characterize  portions  of 


A,  Bowlder  Clay.  B,  Stratified  Red  Clay. 
C.  Stratified  Sand  Deposit,  a,  Obscurely  strat- 
ified bowlder  clay,  b,  Clayey  sand,  c,  Sand, 
d,  Gravel  (bowlders). 


this  deposit.  Contorted  lamina- 
tions, unsurpassed  by  anything  pre- 
sented in  the  metamorphic  rocks, 
are  sometimes  to  be  seen,  closely  associated  with  bowlders,  stratified 
clays,  pockets  of  gravel,  stratified  sand  deposits,  gravel  beds  and  un- 
stratified  hard  pan,  constituting  a  most  changeable  and  irregular  struc- 
ture. The  surface  area  of  this  formation  is  shown  on  Atlas  Plate  IV. 
In  harmony  with  the  irregular  nature  of  this  formation,  the  rock 
here  and  there  was  left  uncovered  by  it,  and  at  some  points  it  was 
swept  away  by  subsequent  agencies,  but  with  these  exceptions,  it  is  to 
be  regarded  as  covering  the  immediate  surface  of  the  rock  over  the 
entire  district. 

MODIFIED  DRIFT  —  CHAMPLAIN. 
I.  BEACH  FORMATION  A. 

During  the  deposit  of  Bowlder  Clay,  there  is  abundant  reason  for 
believing  that  the  general  surface  was  more  elevated  to  the  northward 
than  at  present.  Subsequently,  however,  perhaps  cotemporaneously 
with  the  retreat  of  the  glacier,  and  possibly  also  the  cause  of  its  re- 
cession, there  occurred  a  relative  depression  to  the  northward.  Thia 
depression  was  accompanied  by  a  vast  accumulation  of  water  in  the 


220 


GEOLOGY  OF  EASTERN  WISCONSIN. 


form  of  fresh  water  lakes,  which  are  to  be  regarded  simply  as  the 
expanded  predecessors  of  our  present  great  lakes.  As  this  water  grad- 
ually accumulated  and  advanced  upon  the  land,  it  washed  out  the 
finer  material  of  the  Bowlder  Clay,  carrying  it  backward  into  the  still 
water,  where  it  was  redeposited,  while  it  left  along  the  beach  the 
coarser  sand,  gravel  and  other  material,  forming  a  beach  deposit. 
This  deposit,  to  distinguish  it  from  those  which  subsequently  fol- 
lowed, is  here  designated  Beach  Formation  A.  It  is  abundantly 
exposed  along  the  shore  of  Lake  Michigan,  above  and  below  Milwau- 
kee, where  it  overlies  the  Bowlder  Clay  and  underlies  a  subsequent 
deposit  of  red  clay.  The  accompanying  figure  illustrates  its  relations 

and  relative  thickness. 

FIG.  12. 


W/f/7-£\ 

r/*H    ^  25ft 

B/tY 


53ft. 


28ft. 


Sections  showing  the  relations  and  magnitude  of  the  Bowlder  Clay,  Beach  Formation  A,  and 
Lower  Red  Clay,  at  and  near  Milwaukee. 

The  deposit  consists  chiefly  of  sand,  gravel  and  bowlders,  with  in- 
cluded layers  of  clay.  The  material  is  thoroughly  stratified,  and  ex- 
hibits most  beautiful  and  abundant  examples  of  cross  and  oblique 
laminae,  which  indicate  the  nature  of  its  origin.  The  sand  is  usually 
white  or  yellow,  but  sometimes  ferruginous  or  dark  colored.  The 
constituent  grains  are  of  all  sizes,  from  a  fineness  that  renders  the  mass 
compact  and  almost  plastic,  and  quite  indistinguishable  at  the  dis- 
tance of  a  few  feet  from  the  clay  bands,  to  a  coarseness  that  is  only 
arbitrarily  distinguished  from  gravel.  It  is  banded  and  laminated  in 
the  greatest  variety  of  forms.  Horizontal,  oblique,  undulating,  and 
even  contorted  laminations,  are  present  in  variety. 

The  gravel  exhibits  every  gradation,  from  sand  to  that  which  is  so 
coarse  that  it  is  scarcely  less  than  a  bed  of  boAvlders.  It  is  chiefly 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  221 

composed  of  limestone,  and  is  thoroughly  water-worn,  and  frequently 
shows  an  oblique  arrangement. 

Interstratified  with  these  beds  of  sand  and  gravel  are  bands  of  clay, 
sometimes  quite  pure,  but  more  frequently  arenaceous.  These  are 
usually  finely  laminated,  most  frequently  in  a  horizontal  direction. 
Occasionally  the  clay  develops  to  a  stratum  of  several  feet  in  thick- 
ness, but  more  often  it  only  forms  narrow  bands  alternating  with  the 
finer  grades  of  sand,  which  are  also  more  frequently  laminated  in  a 
horizontal  direction  than  in  the  coarser  kinds,  showing  that  both  were 
deposited  in  comparatively  quiet  waters. 

An  occasional  large  bowlder  occurs  in  the  sand  and  clay  as  well  as 
in  the  gravel.  Small  fragments  of  rock,  usually  subangular,  are 
sometimes  seen  in  the  clay. 

The  formation  is  subject  to  rapid  changes  as  it  is  traced  laterally. 
At  one  point  the  section  may  be  composed  almost  wholly  of  fine  sand 
and  clay,  and  within  forty  rods,  these  may  be  entirely  replaced  by 
coarse  sand  and  broad  bands  of  gravel.  Large  lenticular  masses  of 
sand,  gravel,  or  mixed  material,  are  not  unfrequent.  This  formation 
reaches  a  thickness  of  about  sixty  feet. 

From  its  nature  this  deposit  has  a  very  limited  extent  as  a  surface 
formation.  In  the  abrupt  banks  of  Lake  Michigan,  it  displays  itself 
abundantly,  as  represented  in  plate  VIII,  which  likewise  shows  its 
relation  to  the  overlying  and  inferior  deposits.  Where  it  comes  to  the. 
surface,  it  displays  itself  very  feebly,  and  is  scarcely  distinguishable,  if 
at  all,  at  many  points.  It  forms,  where  present,  a  narrow,  irregular 
belt  between  the  surface  occupied  by  the  Bowlder  Clay  and  that  of  the 
Lower  Red  Clay. 

II.     THE  LOWER  RED  CLAY. 

Lying  upon  the  formation  just  described,  we  find  a  massive  clay  de- 
posit. It  differs  most  obviously  from  the  Bowlder  Clay,  in  possessing 
A  deep  reddish  or  purple  color,  which  weathers  at  the  surface  to  an 
ashy  drab,  while  the  Bowlder  Clay,  although  not  infrequently  reddish 
or  even  purple,  is  usually  blue  or  drab,  and  differs  also  in  the  great  ir- 
regularity of  its  coloration.  Hence  the  formation  in  question  is  ev- 
erywhere known  as  the  "  red  clay.'1'1  It  likewise  differs  from  the  Bowl- 
der Clay  in  respect  to  the  rock  fragments  contained  in  it.  In  the 
Bowlder  Clay  these  are  extremely  abundant,  and  of  all  sizes,  from 
mere  pebbles  to  those  of  many  tons  weight.  In  the  Red  Clay,  where 
they  are  not  entirely  absent,  they  are,  with  rare  exceptions,  small,  sel- 
dom exceeding  six  inches  in  diameter,  and  more  frequently  they  are 
mere  hand  specimens.  The  great  majority  of  these  fragments  are  of 


222  GEOLOGY  OF  EASTERN  WISCONSIN. 

magnesian  limestone,  and  were  apparently  derived  from  the  Silurian 
formations  prevalent  in  the  region.  In  some  instances  this  is  put  be- 
yond question  by  the  occurrence  of  Niagara  fossils  in  them.  The  sur- 
faces and  angles  of  these  fragments  are  worn,  but  not  to  such  an  ex- 
tent, usually,  as  to  give  them  a  symmetrical  rounded  form,  and  it  is 
especially  to  be  noted  that  the  surface  is  scratched  and  subtranslucent 
instead  of  having  an  opaque,  somewhat  granular  surface,  such  as  arises 
from  the  wearing  and  solvent  action  of  water.  Occasionally  a  bowl- 
der of  considerable  dimensions  occurs  within  the  formation,  but  there 
is  a  very  marked  difference  between  this  formation  and  the  Bowlder 
Clay  in  that  respect.  This  fact  becomes  a  very  conspicuous  one  in 
examining  adjacent-  areas,  occupied  by  the  two  formations.  The  sur- 
face of  the  Red  Clay  is  comparatively  free  from  bowlders,  while  they 
occur  in  the  very  greatest  abundance  on  the  surface  of  the  Bowlder 
Clay.  It  may  be  here  remarked  that  there  is  no  such  abundance  of 
bowlders  on  the  surface  of  the  Red  Clay  district  as  to  suggest  any 
other  origin  than  that  of  wash  from  the  formation  itself  *.  The  clay 
which  constitutes  the  chief  element  is  highly  calcareous  in  character. 
It  contains,  also,  a  considerable  portion  of  finely  comminuted  quartz- 
ose  material,  in  addition  to  true  aluminous  clay,  so  that  while  the 
whole  is  quite  compact  and  impervious,  it  yet  has  not  that  extreme 
toughness  and  adhesiveness  that  is  possessed  by  the  typical  aluminous 
•clays. 

A  considerable  ingredient  of  magnetite,  in  the  form  of  minute 
grains,  is  present.  A  magnet  drawn  through  a  handful  of  the  pulver- 
ized clay  usually  brings  forth  more  or  less  of  this  mineral.  Along 
the  lake  shore,  where  the  clay  is  washed  away  by  wave  action,  the 
magnetite  is  left  as  a  deposit  of  black  sand,  mingled  with  the  quartz 
sand  of  the  beach,  whence  it  may  be  collected  in  large  quantities. 
The  lower  part  of  the  deposit  is  usually  very  highly  laminate,  and  pas- 
ses, by  alternations  and  gradations,  into  the  subjacent  beach  deposit. 
The  main  mass  of  the  formation  presents  little  indication  of  the  lines 
of  deposit,  but  upon  close  inspection,  minute  lamination  may  be  ob- 
served. The  relation  of  this  to  the  imbedded  rock  is  interesting.  As 
the  laminae  approach  the  fragments,  the  greater  portion  curve  down- 
ward and  pass  beneath  it,  while  a  portion  curve  over  it.  It  would 
appear  from  this  fact  that  the  fragments  were  dropped  upon  the  sur- 
face of  a  yielding  clay  mass,  and  covered  by  subsequent  deposit.  Near 
the  southern  extremity  of  this  formation,  it  has,  along  the  lake  shore, 
a  thickness  of  from  15  to  20  feet.  At  Whitefish  Bay,  above  Milwau- 
kee, it  is  from  20  to  30  feet  thick,  near  Ulao,  40  feet,  and  in  the  vicin- 

1  Compare  Geological  Survey  of  Ohio,  Vol.  II,  Part  1,  page  4. 


PLATE,  E 


MAP 

Jhotiv'jiy  tAe 

Approximate  Outline 

of 

EASTERN  WIS  CON  SIN 

rtltririff  t/lt- 

Chainplaiu  Period 
•* 

T.  C.  Chaniberlin 
1876. 

Present, 


II  I.ITKO  AfF.HOn.Ro. 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  223 

ity  of  Port  "Washington  it  reaches  its  maximum  observed  thickness  of 
75  feet,  although  it  doubtless  somewhat  exceeds  this  at  some  points. 
At  many  places  along  the  lake  shore,  owing  to  slides  and  washing, 
it  appears  to  have  a  thickness  considerably  exceeding  this. 

It  has  a  wide  surface  distribution,  as  will  be  seen  by  consulting  the 
accompanying  map.  Commencing  near  Milwaukee,  it  widens  to  the 
north  until  the  Kettle  Range  is  reached,  by  which  its  western  boun- 
dary is  deflected  to  the  eastward  until  it  passes  that  barrier  and  swings 
around  upon  the  western  side,  and,  passing  the  watershed,  occupies 
the  Green  Bay  valley.  It  ascends  this  valley  to  a  few  miles  south 
of  Fond  du  Lac,  and  reaches  up  the  Upper  Fox  river  beyond  Berlin, 
while  in  the  Wolf  river  valley  it  extends  beyond  Shawano.  West  of 
the  bay  it  appears  in  much  less  amplitude  than  to  the  southward. 

From  what  has  already  been  said  concerning  this  and  the  underly- 
ing formations,  no  doubt  remains  that  it  was  a  subaqueous  deposit. 
Its  extent  should,  therefore,  indicate  approximately  the  amount  of  the 
encroachment  of  the  lake  at  the  time  of  its  formation,  and  the  alti- 
tudes to  which  it  rises  are  significant  of  the  amount  of  relative  de- 
pression that  attended  its  formation,  and  hence,  an  especial  interest  at- 
taches to  its  vertical  distribution.     At  its  southern  extremity,  it  reach- 
es an  altitude  of  a  little  more  than  100  feet  above  Lake  Michigan. 
Where  its  western  limit  crosses  the  north  line  of  Ozaukee  county  it  is 
about  200  feet.     A  few  miles  east  of  this  it  rises  upwards  of  300  feet. 
At  the  northwest  corner  of  section  36,  town  of  Lynden,  Sheboygan 
count}7,  it  is  315  feet.     In  the  town  of  Rhine,  of  the  same  county,  the 
limit  is  found  at  322  feet;  at  the  middle  of  the  north  line  of  section 
21,  town  of  Memee,  Manitowoc  county,  at  248  feet,  and  on  the  oppo- 
site side  of  the  Kettle  Range,  at  St.  Nazian,  at  the  same  height. 
North  of  this  its  limitation  is  less  w^ell  defined.     There  are  some  in- 
dications that  it  passed  entirely  over  the  Kettle  Range,  in  the  central 
portion  of  Manitowoc  county,  or  at  least  that  the  waters  of  the  period 
did.     Nowhere  north  of  this  was  it  observed  at  a  height  exceeding  330 
feet  above  Lake  Michigan.     Near  Chilton  it  reaches  an  elevation  of 
372  feet;  north  of  Stockbridge,  358  feet;   south,  390;  in  section  6, 
Marshfield,  401  feet;  in  section  5,  Taycheedah  (T.  15,  R.  23),  315  feet. 
These  have  been  selected  from  a  large  number  of  observations,  either 
because  more  reliable,  or  because  more  significant,  on  account  of  their 
positions.     A  more  general  and  comprehensive  appreciation  of  the 
facts  may  be  gained  by  a  comparison  of  the  map  of  Quaternary  For- 
mations with  the  Topographical  map,  both  of  which  will  be  found 
upon  plate  IV,  conveniently  arranged  for  such  comparison.     It  will 
be  observed  that  the  formation  rises  gradually  from  its  southern  ex- 


224  GEOLOGY  OF  EASTERN  WISCONSIN. 

tremity  to  the  region  of  Lake  Winnebago,  beyond  which  it  declines. 
On  Lake  Superior  an  analogous  clay  rises  at  least  one  or  two  hundred 
feet  higher. 

Aside  from  the  general  northward  depression  indicated  by  these 
facts,  a  special  flexure  seems  to  have  taken  place  in  the  region  of  Lake 
"Winnebago,  either  of  the  nature  of  a  greater  depression  during  the 
time  of  deposit,  or  of  a  greater  elevation  subsequently.  This  fact  is 
entirely  in  harmony  with  the  concurrent  indications  of  several  pecu- 
liar features  in  the  underlying  formations  and  general  structure  of  the 
region.  It  is  on  the  basis  of  this  general  northward  depression,  and 
on  the  sequence  of  the  formations,  that  this  and  the  associated  de- 
posits are  referred  to  the  Champlain  period. 

III.  BEACH  FORMATION  B. 

Reposing  upon  the  Lower  Red  Clay,  there  lies  a  deposit  of  sand 
and  gravel,  with  included  layers  of  .clay,  reaching  a  thickness  of  60 
feet  or  more,  and  constituting  a  well  defined  formation.  It  differs  in 
no  essential  respect,  so  far  as  its  character  is  concerned,  from  Beach 
Formation  A,  which  has  already  been  described,  and  hence  it  will  not 
receive  special  description  here.  At  some  points  however,  where  the 
depositing  waters  found  a  rocky  shore,  instead  of  the  accumulations  of 
clay,  sand  and  gravel,  large  blocks  of  the  neighboring  limestone,  more 
or  less  eaten  by  the  waters,  are  strewn  on  the  shore  in  a  manner  sim- 
ilar to  that  which  is  now  being  enacted  on  the  rocky  beach  of  the 
Green  Bay  peninsula  further  north.  The  formation  best  exhibits  itself 
along  the  lake  shore  from  Manitowoc  northward,  where  fine  vertical, 
sections  may  be  seen,  one  of  which  is  illustrated  in  the  accompanying 

figure. 

FIG.  13. 


PROFILE  SECTION  ON  LAKE  SHORE,  NEAR  MANITOWOC. 
1.  Lower  Red  Clay.    2.  Sand  Deposit.    3.  Alternating  Belts  of  Sand  and  Clay. 

It  becomes  a  surface  formation  between  the  Upper  and  Lower  Red 
Clays.  Appearing  upon  the  lake  shore  in  the  vicinity  of  Manitowoc, 
its  surface  exposure  stretches  northward  in  the  valley  of  the  East 
Twin  river  into  Kewaunee  county,  whence  it  curves  slightly  to  the 
eastward  into  the  basin  of  the  Ahnapee  river,  from  the  valley  of  which 
it  passes  over  the  watershed  into  the  Green  Bay  valley,  which  it  skirts 
on  the  east  as  far  south  as  Lake  Winnebago,  whence  it  returns  on  the 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  225 

westward  slope  of  the  valley,  and  runs  north,  parallel  to  its  axis,  until 
it  crosses  the  Menomonee  into  Michigan.  Its  highest  observed  ele- 
vation is  about  200  feet,  in  the  vicinity  of  Lake  Winnebago.  Its  sec- 
tion, as  shown  on  Lake  Michigan,  may  be  seen  on  Plate  YIII  of  this 
volume,  and  its  surface  distribution  on  Plate  IY  of  the  accompanying 
atlas. 

IY.  UPPER  RED  CLAY. 

The  description  that  has  been  given  of  the  Lower  Red  Clay  applies 
almost  completely  to  this  deposit,  the  only  grounds  for  separating 
them  being  the  intervention  of  the  beach  deposit  which  has  just  been 
described.  The  similar  character  of  the  clay,  the  angularity  of  the 
imbedded  fragments  of  limestone,  and  their  un weathered  nature,  the 
high  color  of  the  clay,  the  large  content  of  magnetite,  are  likewise 
characteristic  of  this  formation.  It  covers  the  northeastern  corner  of 
Manitowoc  county,  the  eastern  portion  of  Kewaunee  county  and  the 
adjoining  portion  of  Door  county.  It  doubtless  originally  covered 
the  entire  Green  Bay  peninsula  and  was  apparantly  swept  away  by  the 
action  of  the  lake  as  it  gradually  retired. 

Its  thickness  is  nowhere  considerable.  Along  the  lake  shore  where 
it  is  best  exposed,  and  possibly  thickest,  it  rarely  exceeds  20  feet. 

In  Racine  and  Kenosha  counties,  there  is  a  yellowish  clay  deposit 
quite  similar  in  most  of  its  characteristics  to  the  Red  Clays,  except 
in  its  color  and  the  more  frequent  presence  of  bowlders.  In  addition  to 
the  evidence  drawn  from  the  nature  of  the  deposit  itself,  the  configur- 
ation of  the  country  indicates  the  modifying  action  of  water.  It 
seems  probable  that  this  was  more  immediately  connected  with  the 
melting  and  retreat  of  the  glacier  than  the  formations  above  con- 
sidered. 

Y.  BEACH  FORMATIONS  C  AND  D,  AND  THE  MODIFIED  RED  CLAY. 

Along  the  eastern  border  of  Racine  and  Kenosha  counties,  extend- 
ing on  the  average  about  one  mile  back  from  the  lake  shore,  we  find 
at  the  surface  a  deposit  of  sand  and  gravel,  with  a  varying  but  subor- 
dinate admixture  of  clayey  and  marly  material.  The  gravel  is  usually 
fine  and  thoroughly  waterworn,  and  is  interstratitied  with  the  sand 
and  occasionally  with  clay,  and  almost  everywhere  presents  beautiful 
examples  of  oblique  lamination.  It  rarely  exceeds  twenty  feet  in 
thickness,  and  on  the  average  is  about  half  that  amount.  At  its  base, 
along  the  lake  shore,  numerous  springs  issue,  the  water  being  pre- 
vented from  descending  farther  by  the  impervious  clay  that  lies  below. 
Wis.  SUB.  —  15 


226  GEOLOGY  OF  EASTERN  WISCONSIN. 

These  springs  are  frequently  ferruginous,  as  are  also  certain  bands  of 
the  deposit. 

The  western  limit  of  this  formation  is  marked  by  a  low  flat  ridge, 
usually  only  six  or  eight  rods  in  width,  and  less  than  three  feet  in 
height.  At  most  points,  this  is  composed  of  fine  gravel,  except  near 
the  state  line,  where  it  becomes  sandy.  The  surface  between  this 
beach  ridge  and  the  lake  is  level  and  free  from  bowlders,  but  imme- 
diately to  the  west  of  the  ridge,  small  bowlders  occur,  except  over 
certain  areas  that  are  covered  with  lacustrine  and  fluviatile  deposits. 
Here  and  there  a  stream  has  cut  a  deep,  sharply-defined  gorge  for  it- 
self, but  broad,  sloping  valleys  are  wanting. 

Immediately  beneath  the  above  beach  formation  lies  a  finely  lam- 
inated compact  clay.  It  has  a  prevailing  reddish  hue,  which  is  at 
some  points  pronounced,  but  at  others  is  bluish  or  dark  grayish.  It 
contains  but  few  pebbles  and  very  rarely  anything  that  could  be  de- 
nominated a  bowlder.  The  laminations  are  horizontal  and  often  ex- 
ceedingly fine.  Some  arenaceous  layers  are  usually  present,  especial- 
ly toward  the  top. 

In  the  vicinity  of  "  The  Point,"  near  Racine,  this  clay  rests  di- 
rectly upon  the  Bowlder  Clay.  The  line  of  junction  is  most  sharply 
and  distinctly  marked.  The  surface  of  the  obdurate  hard-pan,  which 
here  constitutes  the  lower  formation  is  sometimes  planed  almost  like 
a  glaciated  surface,  and  the  resemblance  is  enhanced  at  some  points 
by  parallel  lines  of  white  material,  the  significance  of  which  was  not 
ascertained.  In  other  cases  it  presents  an  undulatory  ripple  like  sur- 
face, and  in  still  others  is  more  irregular.  These  observations  are 
made  possible  by  the  distinctness  of  this  hard-pan  from  the  fine  put- 
ty-like red  clay  that  rests  upon  it.  In  digging  it  away,  the  red  clay 
peels  off  from  the  surface  of  the  lower  clay,  leaving  it  perfectly  clean 
and  distinct. 

But  as  we  trace  these  clays  northward  a  stratum  of  yellow  sand 
develops  between  the  two  and  rapidly  increases  in  thickness,  while 
the  red  clay  correspondingly,  but  somewhat  less  rapidly,  thins  out. 
Four  drift  formations  are  well  shown  at  this  point;  a  beach  forma- 
tion (D),  at  the  top,  being  here  a  stratum  of  yellow  sand  only  a  few 
feet  in  thickness,  the  red  clay  (modified)  next,  and  beneath  this 
another  beach  formation  (C),  resting  upon  the  Bowlder  Clay,  as  shown 
in  the  accompanying  figure. 

As  we  advance  northward,  or  more  strictly  northwestward,  the  three 
upper  formations  rise  and  disappear  at  the  surface  in  succession,  each 
seeming  to  have  been  cut  off  above  by  erosion.  This  is  not  accom- 
plished, however,  until  the  thinning  out  of  the  red  clay,  and  the  ap- 


QUATERNARY  FORMATIONS  —  THE  DRIFT. 


227 


proach  of  the  sand  deposits  above  and  below,  toward  each  other,  have 
forced  the  conviction  that  these  latter  really  join  at  points  where  the 
erosion  has  not  taken  place,  and  that  the  beach  ridge  that  I  have 
already  described  marks  their  junction,  and  that  they  enclose  the  red 
clay  deposit  as  an  equitant  leaf  does  its  fellow. 

FIG.  14. 


SECTION  NORTH  OF  "THK  POINT,"  NEAR  RACINE. 

I.  Bowlder  Clay.    2.  Beach  Formation  C.    3.  Modified  Red  Clay.    4.  Beach  Formation  D.    5.  Sup- 

posed  Original  Surface. 

It  seems  clear  that  these  formations  were  produced  by  an  advance 
and  subsequent  retreat  of  the  great  lake.  The  advance  was  attended 
by  a  deposit  of  sand  and  gravel  along  the  beach,  where  the  material 
was  acted  upon  by  the  breakers,  and  by  a  deposit  of  fine,  clayey  ma- 
terial on  the  undisturbed  bottom  off  shore.  This  progressive  move- 
ment continued  until  the  position  of  the  beach  ridge  already  men- 
tioned was  reached,  where  a  halt  was  made  for  a  time,  during  which 
the  ridge  was  thrown  up  by  the  waves,  after  which  the  water  retired, 
but  at  a  higher  level  than  the  line  along  which  it  advanced,  as  would 
be  necessitated  by  the  filling  up  caused  by  the  deposits  made  in  the 
interval.  As  the  lake  retired,  the  upper  beach  deposit  (D)  was  formed, 
and  the  deposit  of  clay  off  shore  continued.  This  explains  com- 
pletely the  cuneate  form  of  the  clay  deposit.  Taken  as  a  whole,  the 
clay  was  synchronous  with  the  beach  deposits,  though  in  any  given 
vertical  section,  it  was  later  than  that  below,  and  older  than  that  above. 

This  will  be  made  more  clear  by  an  examination  of  the  following 
partially  ideal  figure,  illustrating  these  formations. 

FIG.  15. 


1.  Racine  limestone.    2.  Bowlder  Clay.    3.  Beach  formation  C.    4.  Modified  Red  Clay.    5.  Beach 
formation  D.    6.  Beach  formation  in  progress.    7.  Off-shore  clay  deposit  in  progress. 

These  formations  are  isolated  from  the  red  clays  and  beach  deposits 
previously  described,  and  their  relations  to  them  are  not  certainly 
established,  and  therefore  the  provisional  names  originally  assigned 
them  are  retained;  and  in  the  absence  of  demonstrative  evidence,  and 


228  GEOLOGY  OF  EASTERN  WISCONSIN. 

of  sufficient  space  for  the  wide  discussion  of  the  Champlain  deposits 
of  the  great  lake  region,  to  which  a  proper  treatment  of  the  subject 
would  lead,  it  is  deemed  best  to  leave  the  question  for  future  consid- 
eration. 

The  elevation  of  the  oeach  ridge  which  marks  the  western  limit  of 
these  deposits  above  Lake  Michigan  is  as  follows: 

Near  the  Illinois  line 55  feet. 

A  little  farther  north 53    " 

In  Sec.  18,  S.  E.  qr.  T.  1,  R.  23  E 40    " 

In  Sec.  1,  middle  S.  line  S.  E.  qr.  T.  2,  R.  22  E 44    " 

In  Sec.  19,  S.  E.  corner  T.  3,  R.  23  E 80    " 

In  Sec.  29,  S.  E.  qr.  S.  line  T.  4,  R.  23  E 68    " 

TERRACES. 

Just  north  of  the  lighthouse  north  of  Milwaukee,  the  bank  facing 
the  lake  is  low,  but  a  few  rods  back  there  is  a  well  defined  terrace 
running  nearly  parallel  to  the  lake  shore,  and  rising  from  50  to  100 
feet  above  it.  This  continues  northward,  with  interruptions,  for  sev- 
eral miles.  A  similar  terrace  accompanies  the  greater  portion  of  the 
shore  line  between  Port  Washington  and  Sheboygan,  and  near  Cen- 
terville  there  is  a  feeble  development  of  the  same  phenomenon,  beyond 
which  it  is  absent  for  a  considerable  interval.  Just  north  of  Alma- 
pee  the  terrace  reappears  in  sharp  and  rigid  outline,  and  extends  with- 
out essential  interruption  to  the  vicinity  of  Sturgeon  Bay.  It  attains 
in  this  portion  a  height  of  75  feet.  Between  the  terrace  and  the  lake 
a  mature  growth  of  forest  vegetation,  of  a  highly  mixed  character,  is 
to  be  found. 

Beach  Ridge  of  Sand.  In  the  vicinity  of  Sturgeon  Bay,  the  ter- 
race is  replaced  by  a  beach  ridge  of  rather  fine  yellow  sand.  With  lim- 
ited interruptions  this  ridge  extends  to  Port  de  Morts. 

Beach  Ridge  of  Rock-fragments.  As  we  round  the  point  and  re- 
turn on  the  Green  Bay  side,  much  more  frequent  interruptions  occur 
from  the  rocky  promontories  that  characterize  this  shore;  and  instead 
of  being  sandy,  the  ridge  is  here  chiefly  formed  of  chip-stone  with  par- 
tially rounded  angles,  and  of  the  flat  pebbles  that  mark  a  rocky  beach, 
where  the  fragments  are  worn  rather  by  sliding  than  by  rolling. 
These  form  sharp  ridges,  sometimes  rising  20  to  30  feet  above  their 
bases,  on  either  side,  and  become  a  very  conspicuous  feature  at 
Ephraim,  Fish  Creek,  Egg  Harbor,  and  elsewhere. 

Terraces  of  Rock.  Along  this  shore  also,  notably  between  Egg 
Harbor  and  the  mouth  of  Sturgeon  Bay,  terraces  of  rock  sustain  a  re- 
lation to  the  present  shore  altogether  similar  to  that  held  by  the  clay 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  229 

terraces  further  south.  These  rise  in  some  cases  almost  vertically,  to 
a  height  of  more  than  100  feet.  The  distance  between  them  and  the 
bay  varies  from  a  few  rods  to  half  a  mile  or  more,  and  the  interval  is 
strewn  with  water-worn  fragments  of  rock  and  occasional  slight  beach 
ridges. 

The  three  forms  united.  Near  Green  Bay  (Sec.  24,  T.  24,  E.  21  E.) 
there  is  an  inconspicuous  beach  ridge,  formed  of  worn  chip-stone, 
first  appearing  on  the  bay  shore  and  extending  a  few  rods,  when  it  is 
replaced  by  a  well  defined  terrace  of  red  clay,  which  extends  south- 
ward nearly  parallel  to  the  shore  for  about  two  miles,  when  it  is  in 
turn  replaced  by  a  low,  flat,  sandy  ridge,  which  may  be  traced  around 
the  extremity  of  the  bay  and  northward  along  the  western  side  to  the 
Menomonee  and  beyond. 

The  intimate  association  of  the  ridges  and  terraces  here  exhibited, 
and  found  less  conspicuously  elsewhere,  leaves  no  doubt  that  they  are 
only  different  phases  of  the  same  formative  process. 

Between  the  lake  shore  and  the  terrace  of  red  clay  and  of  rock,  the 
surface  does  not  usually  exceed  fifteen  feet  above  the  lake  level.  The 
sandy  ridge  that  succeeds  the  terraces  rises  to  the  northward,  reach- 
ing 44  feet  in  Sec.  9,  T.  33,  K.  29  E.,  being  the  most  northern  point 
at  which  the  elevation  was  taken.  The  rocky  or  gravel  ridge  attains 
a  greater  height. 

At  Hedge  Hog  Harbor  it  is 40  feet. 

At  Big  Sister  Bay 65     " 

At  Eagle  Harbor 53    " 

At  Egg  Harbor 50    " 

At  Fish  Creek 55    " 

The  elevation  becomes  less  again  toward  the  southern  extremity  of 
Green  Bay.  These  elevations  were  all  taken  upon  the  crest  of  the 
ridge. 

Secondary  Beach  Lines.  Between  this  ancient  beach  and  the  pres- 
ent one,  there  is  frequently  a  second  well  defined  ridge  of  lower  ele- 
vation, and  occasionally  a  third.  These  are  sometimes  sandy  and 
sometimes  composed  of  rock  fragments,  like  the  primary  ridges. 

GENERAL  MOVEMENTS. 

The  movements  made  by  the  agencies  which  produced  the  foregoing 
Quaternary  formations  are  of  an  exceedingly  interesting  character. 
There  was  first  the  advance  of  the  great  glacier  through  the  deep 
basin  now  occupied  by  Lake  Michigan,  and  through  the  Green  Bay 
valley.  The  diagram  of  glacial  movements,  given  on  a  previous  page 


230  GEOLOGY  OF  EASTERN  WISCONSIN. 

cannot  be  supposed  to  accurately  represent  the  details  of  the  original 
advance  of  the  glacier,  but  rather  the  movements  at  the  time  of  its 
retreat;  but  there  is  sufficient  evidence  to  warrant  the  general  state- 
ment that  the  original  advance  was  along  the  two  great  valleys  men- 
tioned. Then  came  the  melting  away  and  the  consequent  retreat  of 
the  ice  mass,  leaving  strewn  over  the  surface  the  Bowlder  Clay,  and 
by  a  great  halt  and  advance  in  the  midst  of  its  retreat,  forming  the 
great  morainic  Kettle  Range.  Following  the  retreat  of  the  ice  sheet, 
there  was  an  advance  of  the  lake,  giving  rise  to  Beach  Deposit  A,  and 
the  off-shore  lacustrine  formation,  the  Lower  Red  Clay.  When  this 
advance  had  reached  its  maximum  extent,  the  waters  were  withdrawn, 
apparently  with  much  rapidity,  since  we  find  little  or  no  evidence  of 
beach  action  on  the  surface  of  the  red  clay.  As  to  how  far  the  lake 
retreated  there  is  no  evidence,  but  returning,  it  again  advanced  upon 
the  laud,  but  to  a  less  extent  than  before,  and  in  that  advance,  pro- 
duced Beach  Formation  B,  and  the  Upper  Red  Clay,  as  the  coordin- 
ate oft'  shore  deposit,  after  which  it  again  retired,  leaving  little  or  no 
evidence  of  its  retreat  upon  the  surface.  A  third  time  it  advanced 
but  at  a  lower  elevation.  It  cut  deeply  into  the  previous  deposits, 
whether  of  drift  or  rock,  forming  the  extensive  terraces  that  charac- 
terize the  shores  of  Lake  Michigan  and  Green  Bay.  After  this,  for  a 
third  time  the  lake  retired,  and  is  now  advancing  at  a  still  lower  level. 
These  movements  will  perhaps  be  more  vividly  apprehended  by  con- 
sulting the  accompanying  diagram. 


FIG.  16. 


DIAGRAM  ILLUSTRATING  THE  ADVANCE  AND  RETREAT  OF  THE  LAKE  SHORE,  AND  THE  OSCILLATIONS 
OF  THE  LAKE  LEVEL,  SINCE  THE  GLACIAL  EPOCH. 

The  Moraine  and  the  Bowlder  Clay  were  formed  by  the  Retreating  Glacier.  The  white  bands  through 
which  the  arrows  pass  represent  Beach  Deposits  A  and  3,  and  the  lined  bands,  the  Upper  and 
Lower  Red  Clays. 

It  has  already  been  stated  that  some  of  these  advances  of  the  lake 
were  due  to  relative  depression  of  the  land.  It  becomes  evidently  a 
question  of  the  most  vital  importance  to  ascertain  whether  the  pres- 
sent  advance  is  due  to  simple  erosion,  or  to  a  subsidence  of  the  land, 
and  we  are  thus  led  to  the  subject  of  Lake  Encroachment. 

Encroachment  of  Lake  Michigan.  A  considerable  portion  of  the 
shore  of  Lake  Michigan  is  formed  by  high,  steep  banks  of  clay,  sand 
and  gravel.  These  are  being  continually  undermined,  thrown  down, 
and  borne  away  by  the  restless  activity  of  the  waves.  The  rate  at 


QUATERNARY  FORMATIONS  — THE  DRIFT.  £31 

which  the  land  is  thus  being  swept  into  the  lake  becomes  a  question 
of  importance. 

It  should  be  understood  that  the  lake  is  not  advancing  at  all  points, 
and  that  the  rate  of  its  advance  at  different  points  is  not  uniform. 
The  encroachment  seems  to  be  most  rapid  in  the  neighborhood  of  Ra- 
cine. The  land  at  this  point  projects  into  the  lake,  and  is  thus  more 
exposed  to  the  action  of  the  waves.  To  Dr.  P.  R.  Hoy,  of  that  place, 
I  am  indebted  for  data  and  personal  assistance  in  investigating  this 
subject.  He  had  previously  estimated  the  average  erosion  in  that 
vicinity  at  four  feet  per  year.  The  measurements  given  on  a  subse- 
quent page  show  that  for  the  entire  shore  line  of  the  county  the  ave- 
rage advance  is  3.33  feet,  which  shows  that  the  estimate  of  Dr.  Hoy 
for  the  more  immediate  vicinity  of  Racine,  where  it  is  greater,  cannot 
be  far  from  the  truth. 

As  an  example  of  rapid  erosion,  careful  measurements  of  the  cem- 
etery lot  at  Racine  were  made  and  compared  with  previous  surveys, 
with  the  following  results: 

Length  on  the  lake  shore — 921  feet. 

Width  at  the  south  end 404    " 

Width  at  the  north  end 466    " 

Average  width 435    " 

Amount  of  land  at  present  date,  9.18  acres.  To  this  is  to  be  added 
9  acres  sold  from  the  west  side,  making  18.18  acres.  In  1840,  there 
were  25  acres,  making  a  loss  of  6.82  acres  in  24  years,  or  more  than  a 
quarter  of  an  acre  yearly,  or,  stated  in  an  another  form,  the  lake  has 
been  advancing  at  that  point  the  last  24  years  at  the  rate  of  9.73  feet 
per  year.  The  data  for  this  calculation  were  furnished  by  Dr.  Hoy, 
and  the  measurements  were  made  with  his  assistance.  It  is  not  prob- 
able that  the  erosion  at  any  point  exceeds  this,  and  it  has  recently 
been  checked  by  break- waters. 

The  following  carefully  prepared  data  were  furnished  me  by  Dr. 
Lapham,  and  I  am  glad  to  substitute  them  for  the  less  complete  meas- 
urements made  by  myself. 

"  Mr.  S.  G.  Knight,  of  Racine,  has  carefully  measured  for  the  Geo- 
logical Survey,  from  the  nearest  section  corner  or  quarter  post,  to  the 
bank  of  Lake  Michigan,  along  all  the  section  lines  in  Racine  county, 
the  results  of  which,  compared  with  the  government  survey  made  in 
1836,  are  given  in  the  following  table.  Had  these  measurements  been 
made  at  right  angles  to  the  shore  line,  the  result  would  have  been  a 
trifle  less ;  but  as  some  portions  of  the  bank  have  been  artificially  pro- 
tected, we  may  assume  the  result  as  a  close  approximation  to  the 


232  GEOLOGY  OF  EASTERN  WISCONSIN. 

actual  amount  of  loss,  during  the  past  thirty-eight  years,  in  Eacine 
county.    These  measurements  will  have  their  value  many  years  hence. 


LA.KE    SHORE   IN   RACINE    COUNTY. 


SECTION  LINES. 

1836. 

1874. 

Loss. 

North  line  of  Sec. 

6,  T.  4,  R.  23  .... 

....  32.70 

30.30  . 

2.40 

North    " 

7,  T.  4,  R.  23  .... 

....  34.68 

33.45  . 

1.23 

West     " 

8,  T.  4,  R.  23 

....  30.18 

29.70  . 

0.48 

North    " 

17,  T.  4,  R.  23  .... 

....  16.38 

14.60  . 

1.78 

West     " 

16,  T.  4,  R.  23  .... 

....  10.86 

9.75  . 

1.11 

North     " 

21,  T.  4,  R.  23  .... 

....  15.58 

14.50  . 

1.08 

West     " 

22,  T.  4,  R.  23  .... 

....  19.39 

18.43  . 

0.96 

North    " 

27,  T.  4,  R.  23  .... 

....  26.39 

26.39  . 

0.00 

North    " 

34,  T.  4,  R.  23  

....  16.04 

15.47  . 

0.57 

West     " 

34,  T.  4,  R.  23  .... 

....  31.50 

30.00  . 

1.50 

South    " 

33,  T.  4,  R.  23  

...  28.87 

27.34  J. 

1  53 

North    "        " 

4,  T.  3,  R.  23  

...  28.03 

26.50  > 

North    " 

9,  T.  3,  R.  23  

,  ...  18.82 

18.00  . 

0.82 

North    " 

16,  T.  3,  R.  23  

....  27.80 

20.60  . 

6.20 

North    " 

21,  T.  3,  R.  23  

...  21.25 

18.00  . 

3.25 

North    " 

28,  T.  3,  R.  23  

....  32.22 

31.16  '. 

1.06 

West      "        " 

28,  T.  3,  R.  23  

....  30.20 

23.87  . 

6.83 

North    "        " 

32,  T.  3,  R.  23  

...  34.85 

32.40  . 

2.45 

South     "        " 

32,  T.  3.  R.  23  

...  46.60 

44.73  . 

1.87 

Mean  of  18  places,  chains  

1  92 

12672 

Loss  per  annum 

in  feet  

333 

The  following  measurements  were  made  to  ascertain  the  amount  of 
the  abrasion  of  the  west  shore  of  Lake  Michigan,  in  Milwaukee 
county,  since  the  government  survey  made  in  1835  and  1836. 


PLACE. 

1835. 

Chains. 

1874. 

Chains. 

ANNUAL  Lo 
Feet. 

On  the  South  line  of  Sec.    1,  T.  5,  R.  22 

45.61 

44.50 

1.90 

K 

36,  T.  6,  R.  22 

15.90 

14.40 

2.60 

M 

24,  T.  6,  R.  22 

19.29 

18.70 

1.00 

(( 

21,  T.  7,  R.  22 

8.72 

8.42 

0.50 

(1 

15,  T.  7,  R.  22 

5.37 

2.82 

4.31 

(I 

10,  T.  7,  R.  22 

43.35 

41.64 

2.90 

II 

3,  T.  7,  R.  22 

19.34 

17.36 

3.33 

«( 

34,  T.  8,  R.  22 

22.00 

18.69 

5.61 

Menu  .... 

2  77 

The  loss  in  the  other  counties  bordering  the  lake  is  less  on  the  aver- 
age. 
These  facts  are  sufficient  to  show  the  importance  of  taking  imme- 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  233 

diate  steps  to  save  our  territory  from  the  voracity  of  Lake  Michigan. 
The  question  naturally  arises,  Is  this  advance  of  the  lake  due  to  a 
subsidence  of  the  land  ?  This  question  very  materially  affects  the  value 
of  all  the  property  along  the  shore,  for  if  this  advance  is  due  to  a  sub- 
sidence, it  is  largely  beyond  our  control,  and  where  and  when  it  will 
end  could  only  be  conjectured,  and  it  would  be  practically  useless  to 
attempt  to  permanently  stay  its  progress.  But  fortunately  there  no- 
where appears  to  be  any  evidence  of  such  subsidence.  If  any  consid- 
erable movement  were  in  progress  it  would  doubtless  have  been  no- 
ticed in  some  of  the  harbors,  but  none  has  been  detected. 

It  has  been  shown  above  that  the  entire  Wisconsin  shore  of  the  lake 
has  in  recent  geological  times  stood  from  10  to  50  feet  lower  than  at 
present,  reckoning  the  water  level  as  constant,  or  that  the  lake 
is  now  at  a  lower  level  than  at  that  period.  It  is  also  known  from 
the  same  facts  that  in  a  period  of  years  that  must  be  reckoned  by 
hundreds,  if  not  thousands,  the  lake  has  on  the  whole  made  no  ad- 
vance. Along  120  out  of  200  miles  of  lake  shore  the  present  line  is 
farther  east  than  the  ancient  one,  and  the  territory  of  Wisconsin 
seems  to  be  somewhat  greater  now  than  then.  The  encroachment  is 
hence  not  a  cause  of  grave  apprehension,  although  it  demands  ener- 
getic attention. 

The  material  washed  out  from  the  shore  is  borne  southward  and 
accumulates  rapidly  on  the  north  side  of  all  the  solid  piers,  that  ex- 
tend out  from  the  shore,  forming  triangular  areas  of  "  made  land,"  as 
it  is  termed  with  questionable  propriety. 

DUNES. 

A  few  miles  south  of  Sheboygan,  and  at  several  other  points  along 
the  shore,  the  narrow  area  between  the  ancient  beach  line  just  men- 
tioned and  the  present  one,  is  covered  with  beach  sand  which  the 
winds  are  still  engaged  in  heaping  up  into  dunes,  which  are  being  cut 
and  shifted  after  the  manner  of  that  formation.  From  their  nature 
and  surroundings  they  have  not  and  probably  never  will  become  large 
or  conspicuous,  and  are  mentioned  here  rather  as  a  matter  of  interest 
than  of  importance: 

EROSION  AND  DEPOSIT  IN  PROGRESS. 

Aside  from  the  special  case  of  lake  encroachment  already  mentioned, 
there  is  a  general  work  of  erosion  and  deposit  in  progress,  as  is  patent 
to  the  commonest  observation.  This  work  in  the  soft  drift  deposits 
progresses  easily  arid  rapidly.  The  hills  are  being  swept  down  and 


934  GEOLOGY  OF  EASTERN  WISCONSIN. 

the  depressions  filled  up  or  excavated  deeper,  according  to  tlieir  na- 
ture. The  irregularities  of  the  Kettle  Range  in  particular  are  grad- 
ually losing  their  conspicuous  peculiarities  under  the  gnawings  of  the 
"tooth  of  time."  The  erosion  of  the  later  lacustrine  and  beach  de- 
posits under  favorable  circumstances  is  very  rapid.  We  were  fortun- 
ate enough  to  secure  reliable  data  in  a  striking  instance  of  this  kind 
near  Racine.  The  eroding  agency  is  a  small  rivulet  that  is  usually 
dry  a  portion  of  the  year.  Twenty-eight  years  ago,  according  to  Dr. 
Hoy  and  others,  it  was  the  merest  ditch  across  which  two  logs  and  a 
few  puncheons  formed  a  rude  bridge.  A  resident  informed  me  that 
two  years  earlier  he  was  accustomed  to  drive  across  it  without  diffi- 
culty, no  bridge  having  been  constructed  al  that  time.  At  the  point 
where  the  bridge  is  now  located,  farther  up  the  stream,  the  lake  hay- 
ing cut  away  the  lower  portion,  the  ditch  which  has  been  excavated  ia 
120  feet  across  the  top,  4:0  feet  deep,  and  23  feet  across  the  bottom. 

.Farther  up  the  stream,  a  distance  of  1,350  feet,  the  channel  is  40 
feet  across  the  top,  16  feet  deep  and  15  feet  across  the  bottom.  It 
is  still  a  considerable  trench  at  2,750  feet  from  its  mouth.  Through- 
out it  is  remarkably  uniform  in  character  and  direct  in  course.  A 
very  cautious  and  safe  calculation  shows  the  material  removed  to  have 
exceeded  2,600,000  cubic  feet,  or  more  than  3,400  cubic  yards  per 
year.  It  is  situated  in  a  level  country  and  does  not  seem  to  have 
been  much  assisted  by  freshets. 

The  upper  portion  of  the  material  excavated  is  sand  and  gravel,  an 
ancient  beach  deposit,  the  lower  portion  chiefly  clay.  From  the  sur- 
face of  this  clay  numerous  little  springs  seep  forth  and  moisten  the 
sides  which  slide  down  to  the  bottom  as  soon  as  they  are  in  the  least 
undermined,  and  the  stream  is  thus  constantly  fed  with  silt.  These 
peculiar  conditions  might  seem  to  be  exceptional,  but  they  are  really 
quite  common  in  the  lake  border  region.  The  loss  from  lake  erosion 
is  vastly  increased  by  the  action  of  springs  similarly  situated  in  the 
banks  facing  it.  In  general  it  may  be  said  that  the  erosion  of  these 
later  deposits,  especially  of  the  red  clays  and  the  beach  deposits,  is 
unusually  rapid. 

INDUSTRIAL  VALUE  OF  THE  DRIFT  FORMATIONS. 

By  far  the  most  important  resource  springing  from  the  drift  of 
this  region  has  already  received  consideration.  I  refer  to  our  fertile 
and  enduring  soils.  The  powdering  and  commingling  of  such  a  vast 
variety  of  minerals  by  the  glacial  forces  was  a  process  than  \vhich 
none  could  be  better  suited  to  produce  a  secure  and  permanent  foun- 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  235 

dation  for  agricultural  industries;  a  resource  for  the  many,  not  the 
few  — a  wealth  for  the  people. 

Brick.  Second  only  to  this  in  importance  are  the  building  mate- 
rials furnished  by  this  formation,  prominent  among  which  are  the  de- 
posits of  brick  clay.  These  belong  to  two  classes,  the  light  colored  and 
red  clays.  The  former  are  lacustrine,  or  fluviatile  deposits,  derived  from 
the  wash  and  redeposit  of  the  bowlder  clay,  and  occur  within  the  area 
covered  by  that  formation.  They  are  local  accumulations,  and  are  of 
various  bluish  drab  and  yellowish  hues.  A  portion  of  these  clays 
burn  to  a  beautiful  cream  color,  while  other  portions  become  red. 
The  superiority  of  the  former  in  texture  as  well  as  color  has  almost 
entirely  excluded  the  products  of  the  latter  from  the  market.  The 
second  class,  the  red  clays,  are  simply  those  portions  of  the  red  clay 
deposits  already  described  as  are  sufficiently  free  from  pebbles  for  the 
purpose.  Such  portions  are  almost  invariably  found  at  the  junction 
of  the  beach  formations  with  the  main  clay  deposit.  At  that  horizon 
are  beds  of  clay  and  sand,  and  of  the  two  variously  mingled,  thus  fur- 
nishing the  two  essential  ingredients  of  brick  manufacture  in  the 
most  convenient  proximity  and  association.  Very  frequently  a  stra- 
tum mingled  in  the  proper  proportion  by  nature  may  be  found.  This 
is  a  definite  and  wide  spread  formation,  and  affords  the  most  unlim- 
ited quantities  of  excellent  material. 

Notwithstanding  its  native  red  color,  it  burns  to  a  very  desirable 
white  or  cream  hue.  This  fact  has  very  justly  excited  not  a  little 
surprise,  none  the  less  so  because  a  portion  of  our  light  colored  clays 
burn  red. 

That  the  light  color  of  the  brick  is  not  due  to  the  absence  of  iron 
is  evident  from  the  manifest  presence  of  that  substance  as  the  color- 
ing matter  of  the  clay,  and  this  has  been  confirmed  by  analysis.  It 
has  been  observed  that  the  brick  frequently  contain  small  black, 
glassy  points,  and  it  has  been  thought  that,  in  the  progress  of  burning 
a  process  of  segregation  took  place,  whereby  the  iron  was  concentrated 
in  these  concretions,  and  this  view  was  apparently  confirmed  by  the 
fact  that  the  brick  are  red  up  to  a  certain  stage  in  the  burning.  The 
recent  investigations l  of  Mr.  E.  T.  Sweet  upon  the  Milwaukee  brick 
have  thrown  much  additional  light  upon  the  subject,  though  not 
specifically  applicable  to  the  red  clays,  since  the  brick  of  the  "  Cream 
City"  are  made  from  a  light  colored  clay.  For  the  purpose  of  com- 
parison, Mr.  Sweet  analyzed  a  specimen  of  the  Madison  clay,  which 

1  Paper  read  before  the  Wisconsin  Academy  of  Sciences,  Arts  and  Letters,  February 
15,  1877. 


236  GEOLOGY  OF  EASTERN  WISCONSIN. 

burns  red,  and  a  specimen  of  clay  and  of  pressed  brick  from  Milwau- 
kee, with  the  following  result: 

Milwaukee  Madison    Milwaukee 

Clay.  Clay.  Brick. 

Silica 38.22  75.80  53.78 

Alumina 9.75  11.07  13.21 

Peroxide  of  iron 2.84  3.53  4.92 

Protoxide  of  iron 1.16  .31  .26 

Carbonate  of  lime 23.20  2.45  

Carbonate  of  magnesia 15.83  .17  7. 41' 

Lime(CaO) 3.24  .39  17.71 

Potash 2.16  1.74  1.54 

Soda 65  1.40  .92 

Water  in  composition 1.85  2.16  

Moisture..                                                                .95  1.54  .192 


99.85  99.56  99.94 

1  Magnesia.  *  Loss  on  ignition. 

From  these  analyses  it  appears  that  there  is  even  a  larger  quantity 
of  iron  oxides  in  the  Milwaukee  clay,  that  burns  white,  than  in  the 
Madison  clay,  that  burns  red,  and  that  in  the  white  brick  there  are 
over  five  per  cent,  of  iron  oxides.  It  is  also  to  be  observed  that  the 
Milwaukee  clay  contains  a  very  large  ingredient  of  lime  and  magne- 
sia, of  which  the  Madison  clay  contains  but  little.  In  view  of  these 
facts  Mr.  Sweet  suggests  that  the  ingredients  of  the  clay  enter  into  a 
combination  somewhat  analogous  to  some  members  of  the  amphibole 
group  in  which  the  iron  does  not  manifest  itself  as  a  coloring  material. 

This  view  is  confirmed  by  the  hard  and  often  semi-vitreous  charac- 
ter of  the  brick,  and  by  the  fact  that  the  light  color  is  developed  at 
the  point  of  incipient  vitrification.  It  is  at  least  certain  that  the 
light  color  is  not  due  to  the  absence  of  iron,  but  to  the  manner  of  its 
combination. 

The  red  clays,  as  has  been  already  repeatedly  remarked,  are  highly 
calcareous,  and  from  the  close  similarity  of  the  brick  formed  from 
them  to  the  Milwaukee  product  it  is  evident  that  both  undergo  essen- 
tially the  same  reactions. 

It  is  thought  to  be  entirely  safe  to  say  that  in  quantity,  quality, 
convenience  of  situation  and  facilities  for  shipment,  these  clays  are 
unsurpassed  on  this  continent.  The  superiority  of  the  brick  is  uni- 
versally acknowledged,  and  their  beauty  is  a  matter  of  general  com- 
mendation. The  entire  number  annually  manufactured  is  estimated 
at  50,000,000,  and  the  value  of  the  product  approaches  half  a  million 
dollars.  The  test  and  verdict  of  the  recent  great  fires  has  been  highly 
favorable  to  brick  as  a  building  material,  and  there  can  be  no  doubt 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  237 

that  in  the  near  future  their  use,  already  large,  will    be  vastly  in- 
creased. 

The  following  statistics,  though  incomplete,  will  indicate  the  meth- 
ods, extent  and  local  details  of  the  industry  (1873  and  187-1): 

At  Milwaukee  there  are  six  yards,  at  which  about  24,000,000  brick 
are  made  annually,  which  are  nearly  all  needed  for  the  local  demand. 
The  common  brick  are  sold  at  $12  per  thousand,  and  the  pressed  at 
$25,  the  value  of  the  entire  annual  product  being  about  $300,000.  A 
large  proportion  of  the  brick  are  made  by  machine,  steam  power  be- 
ing used.  The  capacity  of  each  machine  is  about  30,000  brick  per 
day.  The  kilns  consist  of  from  ten  to  twenty  or  more  arches,  each 
arch  numbering  20,000  brick.  The  product  has  the  light  cream 
color,  so  well  known  in  the  market  as  the  characteristic  of  "Milwau- 
kee brick."  They  are  made  from  a  light  colored  clay,  a  modified 
form  of  the  glacial  deposit. 

At  "  The  Point,"  near  Racine.,  two  firms  —  Messrs.  Erskine  & 
Morris,  and  the  Burdick  Bros.  —  manufacture  about  3,500,000  cream 
colored  brick  per  year  from  red  clay  and  a  layer  of  sand  from  the 
overlying  beach  deposit.  Their  kilns  usually  number  from  250,000 
to  500,000.  which  require  from  five  to  seven  days  in  burning.  One 
cord  of  mixed  wood,  at  a  cost  of  about  $5,  burns  about  5,000  brick. 
The  molding  is  done  by  hand,  with  water  instead  of  molding  sand. 
About  forty  hands  are  employed. 

At  Ozaukee  there  are  two  yards  where  fine  cream  colored  brick 
are  manufactured  from  red  clay  derived  from  the  transition  beds  be- 
tween Beach  Formation  A  and  the  Lower  Red  Clay.  The  brick  are 
sold  at  $8  per  thousand. 

At  Sheboygan  Falls  300,000  excellent  cream  colored  brick  are 
burned  annually.  The  kilns  contain  about  150,000  and  require  from 
seven  to  nine  days  in  burning,  consuming  one-half  a  cord  of  beech 
and  maple  wood  per  thousand  brick,  the  cost  of  the  wood  being  $3 
per  cord.  Red  clay,  to  which  twenty  to  thirty  per  cent,  of  sand  is 
added,  is  used.  The  brick  are  molded  by  hand,  and  sell  at  from  $7 
to  $10  per  thousand. 

At  Manitowoc  large  quantities  of  cream  colored  brick  of  good 
quality  are  made  from  sandy  red  clay  associated  with  Beach  Forma- 
tion B.  No  additional  sand  is  required.  The  brick  are  molded  dry 
and  by  hand.  Full  statistics  were  not  obtainable. 

At  Kewaunee  from  75,000  to  100,000  brick  are  annually  made 
from  clay,  of  essentially  the  same  geological  horizon  as  the  above. 
The  product  is  light  colored,  and  is  sold  at  from  $8  to  $10  per  thou- 
sand. 


238  GEOLOGY  OF  EASTERN  WISCONSIN. 

Near  Appleton  Mr.  J.  H.  Carver  burns  about  1,800,000  excellent 
cream   colored    brick   per   year.     A   variegated   red   clay   furnishe,'? 
the  crude  material  which  is  wrought  by  horse  power.     About  three 
tenths  of  a  cord  of  soft  wood,  worth  $2  per  cord,  burns  1,000  brick, 
which  sell  at  $8. 

At  Neenah  two  parties  —  J.  Bailey  and  E.  M.  Hulse— manufac 
ture  about  1,600,000  per  year  from  red  clay,  using  horse  and  hand 
power.  The  former  gentleman  makes  about  25,000  pressed  brick. 
He  uses  six  grinders  and  employs  from  nine  to  twenty  men.  Mr. 
Hulse  has  three  grinders  and  employs  eleven  men.  About  two-fifthu 
of  a  cord  of  soft  wood,  or  one-half  a  cord  of  mixed  wood,  is  con- 
sumed per  thousand  brick,  at  a  cost  of  from  $2  to  $2.50  per  cord. 
The  brick  are  cream  colored,  and  sell  at  $8  per  thousand. 

At  Menasha  there  are  two  firms,  Messrs.  ITolke  &  Schelke,  and  P. 
McFadden.  Both  parties  use  steam  power,  and  Guard's  mixing  and 
molding  machine,  and  make  1,800,000  per  year.  The  clay  is  red,  but 
burns  in  six  days  to  a  light  cream  color,  consuming  one-half  cord  of 
mixed  wood,  which  costs  $2.50  per  cord.  About  thirty  hands  are 
employed. 

At  Clifton  a  yard  producing  1,000,000  per  year  is  owned  by  B.  F. 
Carter,  and  one  making  700,000,  by  II.  Day  &  Co.,  of  Oshkosh,  the 
latter  under  the  superintendence  of  H.  W.  Carter.  Mr.  B.  F.  Carter 
employs  sixteen  hands  and  uses  steam  power,  with  a  Burnham  ma- 
chine. Nine  men  are  employed  at  the  yard  of  Day  &  Co.  The  crude 
material  is  in  the  form  of  beautiful  laminated  red  clay  and  sand.  The 
brick  are  light  colored,  and  are  sold  at  $7  per  M. 

At  Watertown,  from  3,500,000  to  4,000,000  excellent  cream  colored 
brick  are  burned  yearly  by  D.  S.  Chadwick,  and  about  1,000,000  by 
F.  Black.  The  crude  material  is  a  light  colored,  sandy,  fl uviatile  clay, 
about  16  feet  in  depth.  Williams'  tempering  machine  is  used,  and 
the  molding  is  done  by  hand  in  water.  Three  tenths  of  a  cord  of 
wood,  with  one  and  a  half  bushels  of  coal  dust  ground  into  the  clay, 
is  sufficient  to  burn  1,000  brick.  The  coal  dust  effects  a  large  reduc- 
tion in  expense,  and  is  also  used  in  some  of  the  above  mentioned 
kilns.  Mr.  Chadwick  has  ten  pits  for  tempering,  and  employs  forty- 
five  men.  Mr.  Black  has  six  pits  and  employs  eighteen  hands.  The 
brick  bring  from  $7  to  $10  per  M. 

At  Waterloo,  M.  J.  Rood  burns  about  600,000,  and  John  Helms 
from  800,000  to  1,000,000  per  year,  which  are  sold  at  from  $7  to  $10 
per  M.  A  light  colored,  fluviatile  clay  is  used. 

Large  quantities  are  also  manufactured  at  Jefferson,  Ft.  Atkinson, 
Edgerton,  Whitewater,  and  greater  or  less  quantities  at  Johnson's 


QUATERNARY  FORMATION'S  —  THE  DRIFT.  239 

Creek,  Geneva,  Kewaskum,  Jfulheim,  Two  Elvers,  Northelm,  Center- 
mile,  and  doubtless  at  other  points  that  escaped  our  notice. 

Tiles,  for  draining,  are  manufactured  at  Whitewater,  from  a  light 
grayish  blue  clay,  by  Mr.  A.  Y.  Chamberlin.  Pottery  is  also  made 
at  the  same  place  from  a  clay  obtained  in  the  vicinity. 

The  drift  formations  likewise  furnish  abundant  beds  of  sand  of  ex- 
cellent quality  for  building  purposes,  and  of  gravel  suitable  for  roads 
and  other  purposes. 

Magnetic  Iron  Sands.  It  has  already  been  stated  that  the  red 
clay  contains  a  notable  amount  of  magnetite.  As  it  is  eaten  away  by 
the  lake,  the  grains  of  magnetite  accumulate  on  the  shore,  and  form 
what  is  popularly  known  as  "Black  Sand."  Occasionally  a  layer  of 
three  or  four  inches  of  this  may  be  found  almost  free  from  silicious 
sand,  but  usually  it  is  in  thinner  laminae,  or  mixed  in  varying  pro- 
portions with  common  sand.  It  exists  in  greater  or  less  abundance 
along  the  whole  shore  line,  and  the  aggregate  amount  of  it  is  large. 
It  has  never  been  used  for  economic  purposes,  so  far  as  I  can  learn, 
except  as  "  drying  sand,"  before  the  era  of  blotting  paper.  Similar 
accumulations  are  successfully  utilized  in  the  manufacture  of  steel  in 
other  regions,  and  the  value  of  this  deposit  may  be  worthy  of  consid- 
eration. 

SHELL  MARL. 

It  will  be  most  convenient  to  consider  in  this  connection  a  fine  de- 
posit of  shell  marl  that  occurs  in  sections  17,  18,  19  and  20,  town  of 
Pierce,  T.  24,  R.  25,  Kewaunee  county,  around  the  margin  of  a  small 
lake,  and  upon  a  shoal  within  it,  which,  by  recent  drainage  has  become 
an  island.  At  some  points  it  is  mixed  with  peat  and  at  others 
with  alluvium,  but  on  this  island -it  is  almost  perfectly  pure  shell 
debris.  It  is  soft,  light,  porous  and  pulverulent  on  the  surface. 
"When  brought  up  from  beneath  the  water  level,  it  is  a  soft,  somewhat 
granular  and  clay-like  mass.  A  pole  was  thrust  down  nine  feet  with- 
out giving  any  evidence  of  change  in  material.  A  specimen  of  this 
iiarl  gave  on  analysis  by  Mr.  Bode, 

Carbonate  of  lime 86.09 

Carbonate  of  magnesia 7.18 

Silica 1 .48 

Oxide  of  iron  and  alumina 0.10 

Sulphuric  acid 0.44 

Water 1 .67 

Organic  matter   2.95 

100.00 


For  lands  deficient  in  lime  this  will  furnish  the  needed  fertilizer. 


240  GEOLOGY  OF  EASTERN  WISCONSIN. 

In  the  valley  of  the  Mink  river  in  Door  county,  at  White  Clay  lake 
in  Shawano  county,  and,  in  lesser  quantities,  at  other  points,  similar 
accumulations  occur,  usually  associated  with  peat. 

PEAT. 

When  the  glacier  retired  from  our  state,  it  left  its  debris  in  the 
form  of  drift  heaped  up  in  an  irregular  way  over  the  surface,  giving 
rise  to  numerous  depressions  which  soon  filled  with  water,  resulting 
in  lakes  of  various  forms  and  sizes.  It  is  perhaps  not  too  much  to 
say  that  within  our  district,  these  numbered  thousands.  In  most  cases 
they  soon  filled  to  the  brim  and  then  began  to  overflow  their  margin 
at  some  point,  thus  forming  a  channel,  which  was  rapidly  cut  deeper 
and  deeper,  at  the  same  time  draining  the  lake.  As  the  water  became 
shallower,  vegetation  sprang  up  in  the  form  of  reeds,  flags,  rushes  and 
the  so-called  water  mosses,  which,  on  dying,  fell  to  the  bottom  of  the 
lake,  and  being  prevented  by  the  water  from  complete  decomposition, 
accumulated  as  a  peat  deposit.  As  the  draining  continued  ,these  lakes 
became  marshes,  and  a  new  class  of  vegetation  sprang  up,  varying  ac- 
cording to  the  character  of  the  marsh  formed. 

In  the  region  now  occupied  by  prairies  and  by  oak  openings,  the 
marshes  were  occupied  generally  by  members  of  the  grass  or  sedge 
group,  accompanied  with  those  mosses  that  are  usually  found  associ- 
ated in  this  group.  As  the  vegetation  thus  produced  died  with  the 
succession  of  seasons,  it  was  added  to  the  accumulating  peat  deposit. 
In  the  more  heavily  timbered  regions  of  the  state,  the  marshes  usually 
came  to  be  occupied  by  the  swamp-frequenting  conifers,  the  most 
abundant,  of  which  is  the  tamarac.  In  association  with  these  there 
is  everywhere  to  be  observed  a  luxuriant  growth  of  minor  vegetation, 
among  which  the  Sphagnum  mosses  are  most  efficient  in  peat  produc- 
tion. These  have  the  property  of  dying  below  while  growing  densely 
above,  and  thus  they  contribute  to  the  rapid  accumulation  of  vegeta- 
ble debris,  and  for  this  reason  they  take  foremost  rank  as  agents  of 
peat  formation.  They  are  not  confined  in  their  association  to  the  ar- 
boreus  vegetation  named,  but  in  the  region  under  description  are  most 
abundant  in  that  connection. 

In  regard  to  the  amount  of  peat  formed  in  these  several  ways,  the 
order  will  be  the  reverse  of  that  in  which  they  are  named.  The  ac- 
cumulation appears  to  have  been  much  more  rapid  in  the  tamarac  and 
similar  swamps,  than  in  the  open  marshes,  and  as  a  result  the  deposits 
of  these  marshes  are  almost  un  iversally  found  to  be  deeper  than  those 
of  the  other  class.  The  amount  of  accumulation  thai  took  place  in 
the  open  marshes,  after  they  became  such,  was  undoubtedly  much 


QUATERNARY  FORMATIONS  —  THE  DRIFT. 

greater  tlian  the  accumulation  during  the  period  that  they  existed  as 
lakes. 

Aside  from  the  accumulation  of  peat  in  these  extinct  lakes,  deposits, 
arising  in  similar  ways,  took  place  in  wet  localities  in  connection  with 
running  streams,  or  in  wet  valleys,  that  bear  no  evidence  of  having 
once  been  lakes. 

Bearing  in  mind  the  method  of  formation,  it  will  readily  be  antici- 
pated that  great  variety  in  the  character  of  the  peat  will  be  the  result. 
Its  degree  of  decomposition  ranges  from  merely  dead  vegetation  to 
that  which  has  become  thoroughly  disintegrated,  and  the  value  of  any 
given  deposit  will  depend  in  part  upon  its  character  in  this  respect, 
since  the  fibrous  condition  of  peat  is  one  of  the  serious  obstacles  to  its 
profitable  utilization.  It  will  also  be  readily  understood  from  its 
mode  of  origin,  how  impurities  may  become  incorporated  with  it.  On 
the  margin  of  the  marsh,  the  wash  from  the  adjacent  uplands  will  nat- 
urally introduce  more  or  less  of  earth  or  sand,  j^ear  the  bottom  of 
the  bog,  earth  will  naturally  become  incorporated  with  the  peat,  and 
in  those  cases  where  the  surrounding  regions  have  in  recent  times 
been  cultivated,  the  unusual  amount  of  earth  carried  down  by  tho 
waters  will  render  the  entire  surface  of  the  peat  more  or  less  impure. 
That  portion  of  the  peat  which  accumulated  while  the  lake  was  grad- 
ually becoming  drained  to  a  marsh  is  more  or  less  filled  with  the 
shells  of  snails,  and  the  remains  of  other  animals  that  inhabited  the 
lake.  In  many  cases  the  amount  of  accumulation  of  this  kind  is  very 
considerable,  sometimes  equaling  and  occasionally  surpassing  the  ac- 
cumulation of  the  peat  itself,  forming  a  mixture  of  marl  and  peat 
that  will  prove  very  serviceable  as  a  fertilizer.  "Where  the  peat  accu- 
mulated in  the  vicinity  of  running  streams,  their  periodical  overflow 
has  contaminated  the  deposit  in  a  greater  or  less  degree.  A  fourth 
source  of  impurity  arises  from  travertine,  or  calcareous  tufa,  deposited 
from  springs.  This,  while  it  is  detrimental  to  peat  as  fuel,  enhances 
its  value  as  a  fertilizer.  Hence,  in  the  selection  of  peat  marshes, 
those  which  have  been,  from  their  situation  and  nature,  sheltered  from 
these  sources  of  impurity,  will,  to  that  extent,  be  favorable  to  a  pure 
deposit.  The  situation  and  the  nature  of  the  marsh  will  also  furnish 
some  indication  as  to  the  abundant  presence  or  comparative  absence 
of  the  acids  which  interfere  with  the  direct  use  of  peat  as  a  fertilizer. 
The  character  of  the  vegetation  growing  upon  the  bog  will,  however, 
be  a  more  reliable  indication  of  this.  The  presence  of  shells  or  marl 
may  be  taken  as  satisfactory  evidence  of  the  absence  of  any  harmful 
quantity  of  these  acids.  The  number  of  deposits  of  peat  within  this 
portion  of  the  state  is  very  great,  and  their  purity  ranges  through  all 
Wis.  SUR.  — 16 


24.2  GEOLOGY  OF  EASTERN  WISCONSIN. 

degrees,  from  a  very  slight  impurity,  to  that  which  is  more  properly 
denominated  muck.  The  depth  of  these  deposits  is  also  exceedingly 
varying.  In  the  investigations  of  the  survey,  an  auger  capable  of 
penetrating  12  J  feet  was  used.  In  most  of  the  peat  deposits  occupy- 
ing open  marshes,  this  was  found  sufficient  to  penetrate  to  the  bottom. 
In  most  of  those  arising  from  the  sphagnum  mosses  in  the  forest 
region,  the  depth  was  found  to  exceed  that  amount.  In  some  cases 
marshes  were  said  to  have  a  depth  of  two  or  even  three  times  that 
amount.  The  quantity  of  peat  in  eastern  Wisconsin  is  to  be  reckoned 
by  millions  of  tons. 

Details  of  Borings.  The  first  marsh  tested  occupies  portions  of  sections  28,  29,  30 
and  32,  town  of  Whitewater  (T.  4,  R.  15  E).  Ten  borings  were  made  along  two  lines, 
one  across  the  marsh  and  one  longitudinally. 

1.  The  first  boring  was  on  a  springy  elevation,  near  the  center  of  section  32,  from 
which  the  line  stretched  northward  across  the  marsh.    The  peat  at  this  point  was  very- 
much  mixed  with  shells,  travertine,  and  apparently  some  argillaceous  material.    Sandy 
clay  was  reached  at  a  depth  of  11  feet  4  inches.    A  ditch  near  by  exposed  a  washed  sur- 
face of  the  upper  portion  from  which  were  taken  fresh  water  shells  of  the  genera  Spheer- 
.ium  Planorbis,  Limnsea,  and  Pupa,  the  smaller  species  of  these  genera  being  very 

abundant,  the  larger,  rare.  This  shows  that  the  peat  is  of  lacustrine  origin,  and  that  at 
no  distant  day  this  has  been  a  lake. 

2.  At  50  rods  from,  the  first  boring,  we  find  about  equal  proportions  of  shell-marl  and 
peat.    The  following  is  the  section: 

Soft,  watery,  dark  reddish,  marly  peat 4  ft.  6  in. 

Thin  layer  of  whitish  marl 2  in. 

Peat  as  above 1  ft. 

Hard,  well  decomposed  peat 4  ft. 

Bluish  clay,  filled  with  pebbles  at 9  ft.  8  in. 

3.  The  third  boring  gave  the  following  section : 

Marly  peat 4  ft. 

Hard,  compact  peat 5  ft.  6  in. 

Clay  at 9  ft.  4  in. 

The  bottom  of  a  ditch  near  by  contains  calcareous  sand,  evidently  washed  from  the  peat. 

4.  The  fourth  boring  gave  8  ft.  8  in.  of  reddish,  partially  decomposed  marly  peat,  con- 
taining shells.    Bottom  blue  clay  as  before. 

A  section  exposed  by  a  ditch  between  borings  4  and  5  gave  2  ft.  of  peat,  succeeded 
by  4  in.  of  shell-marl  mingled  with  peat. 

5.  The  fifth  boring  showed  2  ft.  of  moderately  decomposed  marly  peat  as  before,  3  ft. 
somewhat  more  compact,  with  hard  blue  clay  at  5  ft. 

The  remaining  borings  were  on  aline  from  the  S.  E.  qr.  of  the  S.  W.  qr.  of  sec.  29,  to 
the  N.  W.  corner  of  the  S.  W.  qr.  of  sec.  29. 

6.  The  first  two  borings  were  made  to  ascertain  the  structure  of  a  mound  6  feet  high 
and  about  50  feet  in  diameter.    The  boring  at  the  base  gave  3  feet  of  muck-like  peat, 
with  clay  below;  that  in  the  top  of  the  mound  gave  7  feet  8  inches  of  peat,  mingled  with 
much  travertine,  with  clay  and  sand  mingled  at  the  bottom,  which  is  about  \%  ree^ 
above  the  bottom  of  the  boring  at  the  base,  showing  an  accumulation  of  sand  and  clay 
beneath  the  mound,  which  undoubtedly  owes  its  origin  to  a  spring. 


QUATERNARY  FORMATIONS  — THE  DRIFT.  213 

7.  Thirty  rods  farther  west,  the  chief  boring  showed  8  feet  4  inches  of  wateiy,  partially 
decomposed  peat,  free  from  noticeable  travertine  or  marl.    Bottom,  blue  clay. 

8.  The  fourth  boring,  60  rods  from  the  last,  showed  5  feet  6  inches  of  wateiy,  partially 
decomposed  peat,  3  feet  6  inches  of  a  compact,  close  textured,  reddish,  well  decomposed 
peat,  with  blue  clay  at  9  feet. 

9.  The  fifth  boring  showed  a  similar  section,  blue  clay  with  shells  being  reached  at 
8  feet  4  inches. 

The  lower  compact  peat  of  the  last  two  sections  presented  all  the  physical  appearances 
of  superior  quality,  being  apparently  free  from  the  calcareous  material  found  so  abun- 
dant in  the  first  series.  The  marly  peat  will  undoubtedly  prove  a  good  fertilizer,  and 
is  well  adapted  to  the  sandy  soil  of  the  neighboring  farms. 

At  the  head  of  Lake  Geneva  there  is  a  small  area  of  similar  marly  peat,  8  feet  deep. 

In  section  20,  town  of  Sugar  Creek  (T.  3,  R.  16  E.),  there  is  a  peat  marsh  about  one- 
fourth  of  a  mile  wide,  which  extends  eastward  for  several'  miles,  but  is  narrow.  To  the 
westward  it  widens  and  connects  with  an  extensive  marsh  in  the  town  of  Richmond. 
The  following  is  a  typical  section  from  the  center  of  section  20: 

1.  Surface  black  and  somewhat  earthy. 

2.  Well  decomposed,  dark  peat  of  moderate  compactness 5  ft. 

3.  Firm,  well-decomposed  peat 4  ft. 

4.  Drab  clay,  mingled  with  peat,  at 9  ft. 

The  narrowness  of  the  marsh  at  this  point,  and  its  evident  exposure  to  wash  from  the 
neighboring  land,  render  it  probable  that  a  portion  of  the  firmness  of  this  peat  is  due  to 
very  fine  silt,  that  could  not  be  detected  by  sight  or  touch.  At  other  points  the  surround- 
'  ings  were  more  favorable. 

Horicon  marsh  was  tested  near  its  south  end,  with  the  following  meager  results: 

First  Boring  — 

1.  Surface,  loamy  peat. 

2.  Coarse  undecomposed  peat 2  ft.  6  in. 

3.  Black  peaty  clay 1  ft.  6  in. 

4.  Blue  clay 1ft. 

5.  Gravel  at 5  ft. 

Second  Boring  — 

1.  Peaty  soil 1  ft. 

2.  Yellow  clay 3  ft. 

3.  Blue  clay,  lower  part  sandy 2  ft.  6  in. 

4.  Gravel  at 6  ft.  6  in. 

Third  boring  essentially  the  same.  Probably  other  portions  of  the  marsh  would  show 
more  peat. 

A  marsh  near  Berlin,  the  peat  of  which,  I  was  informed,  had  received  a  favorable  opin- 
ion from  judges  at  the  east,  was  tested.  It  lies  along  the  Fox  river,  whose  inundation 
must  be  supposed  to  affect  its  quality.  Three  out  of  several  borings  will  represent  its 
nature : 

First  Boring  — 

1.  At  1  ft.  6  in.,  fibrous,  not  well  decomposed. 

2.  At  3  ft.  6.  in.,  fibrous,  not  well  decomposed,  yellowish  brown. 

3.  At  5  ft.  6  in.,  better  decomposed,  reddish. 

4.  At  6  ft.,  dark  greenish  blue  clay. 

5.  At  6  ft.  6  in.,  clayey  sand. 


244  GEOLOGY  OF  EASTERN  WISCONSIN. 

Second  Boring  —  near  river  — 

1.  At  1  ft.,  fibrous,  loose,  dark. 

2.  At  3  ft.,  layer  of  decomposed  wood. 

3.  At  3  ft.  6  in.,  clay  as  above. 
Third  Boring  —  near  center  of  marsh  — 

1.  At  1  ft.,  dark,  fine  fibrous,  soft,  not  well  decomposed. 

2.  At  3  ft.  6  in.,  less  fibrous,  reddish. 

3.  At  5  ft.  9  in.,  clay  as  above. 

One  of  the  more  interesting  of  the  smaller  marshes  is  found  in  the  W.  hf .  of  sec.  30. 
Beaver  Dam  (T.  11  N.,  R.  14  E.).  There  are  perhaps  80  acres  of  available  peat.  It  is 
surrounded  by  timber  and  has  no  stream  flowing  through  it,  and  was  formerly  a  lake,  as 
shown  by  the  shells  of  Sphserium,  Paludina,  and  Helix,  found  in  the  underlying  clay.  At 
8  rods  from  the  edge,  there  were  4  feet  of  firm,  dry,  reddish,  well  decomposed  peat,  un- 
derlaid by  clay.  Thirty  rods  from  the  edge,  the  following  section  was  obtained: 

1.  At  3  feet,  firm  peat  struck;  that  above,  soft. 

2.  At  5  feet  6  inches,  reddish,  well  decomposed  peat. 

3.  At  7  feet,  firm,  color  of  brown  paper. 

4.  At  12  feet,  clay  and  peat  mixed. 

At  the  centre  of  marsh : 

1.  Upper  portion  as  above. 

2.  At  6  feet,  firm,  red,  fairly  decomposed,  apparently  derived  from  wood. 

3.  At  12  feet  (length  of  auger),  bottom  not  reached;  material  muck  resembling 

brown  paper  pulp;  contained  the  shells  mentioned  above. 

In  the  town  of  Calamus  (T.  11,  R.  13  E.),  N.  W.  qr.  of  sec.  25,  and  S.  W.  qr.  of  sec. 
24,  lies  a  marsh  of  200  acres.  A  small  stream  flows  through  it.  The  following  may 
represent  five  borings  of  similar  import: 

1.  At  2  feet,  well  decomposed,  firm,  black. 

2.  At  3  feet,  well  decomposed,  firm,  black. 

3.  At  5  feet,  well  decomposed,  firm,  yellow. 

4.  At  5  feet  9  inches,  well  decomposed,  firm,  color  brown  paper. 

5.  At  7  feet,  well  decomposed,  firm,  color  brown  paper. 

6.  Blue  marly  clay,  containing  shells. 

The  peculiar  brown  material  was  found  to  be  sandy  in  two  of  the  borings. 
In  the  town  of  Lake  Mills,  sees.  1  and  2,  a  large  marsh,  partially  covered  with  tama- 
rac,  gave  the  following  sections : 

First.  —  Nine  rods  from  the  edge : 

1.  At  4  feet,  dark,  well  decomposed. 

2.  At  7  feet  6  inches,  dark,  well  decomposed. 

3.  At  10  feet,  reddish,  woody,  sandy. 

4.  At  11  feet,  sandy,  blue  clay. 

Second.  —  Forty  rods  from  the  edge : 

12  feet  of  soft,  wet,  not  well  decomposed,  dark,  reddish,  woody  peat. 
No  evidence  of  sand;  bottom  not  reached. 

Third.  —  Nearer  the  edge : 

1.  At  6  feet,  firm,  half  decomposed,  dark  reddish,  woody  fiber. 

2.  At  10  feet,  dark,  well  decomposed,  firm,  apparently  excellent. 

3.  At  12  feet,  sandy;  bottom  not  reached. 

As  an  example  of  the  greater  depth  in  tamarac  marshes,  I  may  give  the  section  ob- 


QUATERNARY  FORMATIONS  —  THE  DRIFT.  215 

tained  in  the  smallest  marsh  tested  during  the  summer,  consisting  of  only  a  few  acres, 
in  W.  hf.  of  S.  E.  qr.  of  sec.  11,  Summit  (T.  7,  R,  17  E.).  It  was  tested  within  six  or 
eight  rods  of  the  edge,  with  the  following  result: 

1.  At  6  feet  6  inches,  began  to  be  wet.  • 

2.  At  10  feet  8  inches,  spongy,  undecomposed  mosses. 

3.  At  11  feet  8  inched,  still  in  peat;  bottom  not  reached. 

Tested  in  a  dry  ditch,  nearer  the  edge,  to  a  depth  of  over  13  feet,  without  finding 
bottom. 

The  foregoing  may  be  taken  as  representing  the  average  character 
of  the  open  peat  bogs  of  the  region.  There  are  deeper  and  more  ex- 
tensive deposits  than  the  ones  given  —  the  selection  of  those  to  be 
tested  having  been  controlled  by  the  necessities  of  other  departments 
of  the  survey. 

Peat  has  been  used  in  this  region  to  some  extent  as  a  fertilizer, 
and  always  with  good  results.  Its  value  is  much  increased  when 
mingled  with  other  kinds  of  fertilizers,  and  it  is  especially  efficient 
in  absorbing  the  liquid  manures  that  are  usually  wasted.  The  good 
results  of  the  few  trials  that  have  been  made,  corroborated  as  they  are 
by  experience  elsewhere,  and  justified  by  reasoning  from  the  nature 
of  the  peat,  commend  this  subject  to  the  earnest  attention  of  our  agri- 
culturists. In  reference  to  the  last  point,  I  may  be  allowed  to  pre- 
sent succinctly  those  properties  of  peat  that  render  it  valuable  as  a 
manure,  chiefly  on  the  high  authority  of  Prof.  S.  W.  Johnson: 

1.  It  absorbs  moisture  both  as  a  liquid  and  a  vapor,  and  so  coun- 
teracts the  effects  of  droughts,  and  makes  it  invaluable  to  the  more 
arid  soils.     This  hygroscopic  property  indicates  a  natural  adaptation 
to  use  as  a  fertilizer  rather  than  as  a  fuel,  it  being  detrimental  in  the 
latter  respect. 

2.  It  improves  the  texture  of  the  soil. 

3.  By  its  decay  it  furnishes  ammonia  and  carbonic  acid,  and  some 
mineral  substances. 

4.  It  assists  in  the  disintegration  of  other  substances  in  the  soil. 

5.  It  absorbs  ammonia  from  the  air,  and  thus  furnishes  it  to  the 
plants. 

6.  By  its  dark  color  it  absorbs  heat  from  the  sun,  and  thus  in- 
creases the  temperature  of  the  soil. 

Attempts  have  been  made  to  utilize  it  as  a  fuel  at  several  points 
with  varying  success.  In  almost  all  cases  it  seems  to  have  furnished 
a  very  fair  fuel,  and  in  some  cases  it  is  claimed  to  be  equal  to  the 
best  hard  wood.  The  general  tenor  of  the  results,  where  machinery 
has  been  used,  is  unfavorable;  where  the  simpler  methods  have  been 
employed,  the  prospect  is  more  encouraging.  In  reference  to  the 


246  GEOLOGY  OF  EASTERN  WISCONSIN. 

•want  of  entire  success  in  the  former  case,  I  gather  the  following 
causes: 

1.  Too  much  is  expected,  and  consequently  too  great  expense  is 
incurred  and  too  great  risks  taken.     Theoretical  calculation  readily 
shows  immense  profits,  and  leads  to  manufacturing  on  a  false  basis, 
unless  large  deductions  are  made  for  practical  difficulties,  and  larger 
margins  left  for  unforseen  contingencies.     The  manufacture  of  peat 
in  this  state  should  only  be  undertaken  on  the  basis  of  reasonable,  not 
immense,  profits,  as  the  result  of  judicious  and  careful  management. 

2.  The  price  of  other  kinds  of  fuel  in  some  places  leaves  too  small 
a  margin  for  profit. 

3.  Errors  in  the  selection  of  the  marsh.     The  simple  existence  of 
peat  of  a  suitable  depth  does  not  ensure  a  suitable  quality.     The  eye 
and  the  fingers  often  reveal  fatal  impurities,  and  of  those  that  pass 
the  examination  of  the  senses,  chemical  analysis  will  show  that  some 
are  unsuitable.     The  proximity  of  a  stream  that  habitually  inundates 
the  bog  is  a  prima  facie  cause  for  suspecting  the  peat  to  be  impure. 

4.  Errors  arising  from  using  that  which  is  too  near  the  edge,  top, 
or  bottom  of  the  bed.     The  edge  and  bottom  are  impure  for  obvious 
reasons.     Before  the  surrounding  country  was  cultivated,  the  top  w;is 
as  pure  as  other  portions;  but  cultivation  has  immensely  increased 
the  amount  of  earthy  material  carried  into  our  marshes  by  the  water, 
and  thus  rendered  the  surface  peat  more  impure. 

5.  Errors  in    the   manufacture.      Prominent  among  these  is  the 
failure  to  suitably  dry  the  peat.     Much  of  it  contains,  when  taken 
from  the  bed,  ni/tiety  per  cent,  of  water.     This  must  be  reduced  to 
about  twenty  before  it  becomes  suitable  fuel.     The  peculiar  hygro- 
scopic property  of  peat,  which  is  one  of  its  valuable  qualities  as  a 
fertilizer,  is  a  source  of  difficulty  here.     Our  dry  and  windy  climate 
is  however  favorable,  and  if  this  difficulty  has  been  overcome  else- 
where, it  may  most  assuredly  be  here. 

6.  Want  of  the  best  conveniences  for  burning  it.     Our  stoves  and 
furnaces  are  especially  adapted  to  coal  or  wood,  and  although  peat 
may  be  used  in  either,  it  is  placed  at  a  disadvantage.     It  must  com- 
pete with  them  on  their  own  ground. 

7.  Want  of  knowledge  on  the  subject,  and  a  natural  indisposition 
to  change  habits. 

These  and  other  errors  will  readily  be  corrected  by  experience,  and 
if  the  laudable  efforts  that  are  being  made  to  develop  this  new  source 
of  fuel  are  sustained  and  encouraged  by  an  enterprising  public  spirit, 
we  may  confidently  anticipate  a  final  success. 


GEOLOGICAL  STRUCTURE  OF  EASTERN  WISCONSIN. 


247 


GEOLOGICAL  STRUCTURE  OF  EASTERN  WISCONSIN. 

The  rocks  of  the  district  under  consideration  consist  of  two  great 
classes,  widely  distinguished  in  age  and  character.  The  more  ancient 
one  consisted  originally  of  sedimentary  materials  which  were  subse- 
quently metamorphosed  into  quartzites,  granites,  porphyries  and  sim- 
ilar rocks,  and  were  folded  and  tilted  at  various  angles.  These  (for- 
merly known  as  Azoic  or  Eozoic)  constitute  the  Archaean  'formations. 
Upon  these  were  afterwards  deposited  a  series  of  sandstones,  shales 
and  limestones  that  have  remained  essentially  unaltered  and  undis- 
turbed to  the  present  day,  which  constitute  the  Paleozoic  formations. 

The  following  table  exhibits  in  their  natural  order  the  formations 
that  will  claim  our  attention: 


HAMILTON, 

LOWTER  HELDERBERG, 

NIAGARA,  - 

CINCINNATI,   - 
GALENA,     - 
TREXTON, 
ST.  PETERS, 
LOWTER  MAGNESIAN, 
POTSDAM,   - 

HUKONIAN,     - 
LATJRENTIAN, 


Devonian, 
[•  Upper  Silurian, 


.  Lower  Silurian, 


Archcean. 


ES 


-  § 
O 
i— i 
O 


248  GEOLOGY  OF  EASTERN  WISCONSIN. 


CHAPTEE  YL 
ARCHAEAN  FORMATIONS. 

The  district  under  consideration  is  occupied  almost  exclusively  by 
Paleozoic  formations.  The  Archaean  rocks  form  the  great  sloping 
floor  upon  which  these  later  deposits  rest,  and  rise  to  the  surface  along 
their  northern  border.  But  the  Archaean  surface  is  very  irregular, 
and  here  and  there  knobs  rise  through  the  superincumbent  formations, 
giving  rise  to  isolated  hills  of  quartzite,  porphyry  and  granite  in  the 
midst  of  the  areas  of  later  rocks.  It  is  to  these  protruding,  but  not 
intrusive, masses  that  our  attention  will  be  chiefly  confined. 

Along  their  northern  border,  the  Paleozoic  formations  lap  upon  an 
immense  series  of  granitic  and  allied  rocks,  that  will  receive  due  con- 
sideration in  the  several  reports  upon  the  Archaean  regions.  They  are 
here  referred  to  as  a  convenient  point  of  departure  in  describing  the 
isolated  areas  above  referred  to,  whose  main  importance  depends  upon 
their  position  with  reference  to  this  Archaean  region,  and  their  rela- 
tions to  subsequent  formations. 

THE  MUKWA  GRANITE. 

The  isolated  outlier  found  in  the  S.  E.  qr.  of  the  K.  E.  qr.  of  Sec. 
26,  and  the  N".  W  qr.  of  the  S.  W.  qr.  of  Sec.  25,  town  of  Mukwa, 
Waupaca  county,  lies  nearest  the  main  Archaean  area.  This  outcrop 
seems  to  have  been  unknown  to  the  geologists  heretofore,  and  came 
to  my  attention  through  information  derived  from  Mr.  Carr,  of  New 
London. 

It  consists  of  three  large,  and  as  many  small,  rounded,  elongated, 
dome-like  outliers,  arranged  nearly  in  a  line  trending  "W.  35°  to  40° 
]ST.,  and  rising  near  the  center  to  a  height  of  nearly  70  feet. 

The  rock  consists  chiefly  of  red  feldspar,  with  which  is  associated  a 
less  quantity  of  quartz  and  a  small  and  varying  amount  of  a  dark 
mineral,  which  was  not  seen  in  the  distinct  crystalline  form,  but 
which  seemed  to  be  an  aggregation  of  minute  blended  blades  of  bio- 
tite.  The  crystals  of  feldspar  are  never  large,  seldom  exceeding  a 
quarter  of  an  inch  in  length,  and  are  usually  quite  minute,  so  that 
some  portions,  from  which  the  dark  mineral  is  absent,  closely  resemble 


ARCH^IAN  FORMATIONS.  249 

red  quartzite  in  appearance.  The  rock  is  intersected  in  various  direc- 
tions by  veins  of  quartz.  It  is  also  cut  into  pyramidal  masses  by 
smooth,  straight  fissures,  which  are  usually  inclined  at  an  angle  of 
from  60°  to  85°  to  the  horizon.  In  trend  these  fissures  constitute  three 
groups :  the  first  nearly  north  and  south ;  the  second  nearly  east  and 
west;  and  the  third  northwest  and  southeast.  There  are  also  large 
irregular  fissures,  and  occasionally  points  are  to  be  observed  from 
which  an  unusual  number,  both  of  the  smooth  and  the  irregular  ones 
seem  to  radiate. 

The  rock  is  very  little  affected  by  weathering,  and  affords  an  excel- 
lent building  material,  though  the  form  of  the  blocks  is  unfavorable, 
and  it  is  somewhat  hard  to  dress. 

No  rock  was  found  in  contact  with  it,  but,  about  half  a  mile  to  the 
southeast,  in  the  line  of  its  trend,  the  Lower  Magnesian  limestone  ap- 
pears, into  whose  horizon  the  outcrop  rises,  though  it  lies  chiefly  in 
that  of  ihe  Potsdam  sandstone,  as  shown  in  the  accompanying  profile. 

FIG.  17. 


PBOFILE  SECTION  SHOWING  THE  RELATIONS  ov  THE  MUKWA  GRANITE. 
1.  Outlier  of  Granite.    2.  Potsdam  Sandstone.    3.  Lower  Magnesian  Limestone. 

THE  BERLIN  PORPHYRY. 

At  Berlin,  thirty  miles  south  of  the  above,  we  next  find  an  out- 
standing Archaean  mass,1  consisting  of  three  large  elongated  domes 
arranged  en  echelon,  bearing  northeast.  The  rock  is  composed  essen- 
tially of  small  crystals  of  orthoclase  feldspar  dissiminated  through 
a  peculiar  cryptocrystalline  base  of  felsite  and  quartz,  forming  a 
quartz-porphyry.  The  crystals  of  feldspar  are  usually  grayish  before 
weathering,  becoming  reddish  afterward.  The  base  in  its  unweath- 
ered  state  very  much  resembles  quartzite,  and  is  of  dark  grayish  cast 
with  a  very  slight  reddish  tinge,  so  modified  by  its  translucency  as  to 
give  to  the  whole  what  may  be  called  a  water  hue.  Yery  thin  splint- 
ers may  be  fused  before  the  blow-pipe  with  difficulty,  forming  a 
transparent  glass-like  bead.  The  effect  of  weathering  is  marked  and 
peculiar.  The  color  changes  to  a  light  reddish,  pinkish,  or  grayish 
white,  and  occasionally  to  a  bright  red,  while  the  mass  becomes  opaque 
and  finely  granular,  and  so  soft  as  to  be  easily  cut.  There  are  occa- 
sionally spots,  streaks,  or  leaves  of  dark  material  in  the  base,  which 

1  Comp.  Dr.  PercivaTs  Report  of  1856,  p.  106. 


250  GEOLOGY  OF  EASTERN  WISCONSIN. 

are  doubtless  the  portions  referred  to  by  Dr.  Percival  as  "  interlami- 
iiated  hornblende  and  mica." 

The  rock  is  very  uniform  in  character  at  all  points  exposed.  It 
presents  an  obscure  parallel  structure  giving  rise  to  a  somewhat  defi- 
nite system  of  cleavage,  but  traces  of  distinct  bedding  were  not  ob- 
served. The  mass  is  traversed  by  extensive  fissures  which  are  readily 
arranged  into  three  groups,  the  predominant  one  of  which  bears  IS". 
W.,  and  the  smaller  ones  E.  of  K  and  K  of  E.,  respectively,  thus 
dividing  the  horizon  into  nearly  equal  arcs;  but  none  seem  to  be  de- 
pendent on  the  cleavage  structure  of  the  rock. 

FIG.  18. 


EAST  AND  WSST  SECTION  THROUGH  THE  BERLIN  POKPHYBY. 
1.  Porphyry.    2.  Potsdam  Sandstone.    3.  Lower  Magnesian  Limestone. 

On  the  south  slope  of  the  hill,  and  within  a  few  rods  of  the  expo- 
sure of  porphyry,  occurs  a  sandstone  in  which  are  imbedded  masses 
of  the  porphyry  of  various  sizes.  The  sandstone  also  contains  several 
species  of  Potsdam  fossils,  demonstrating  the  presence  of  the  por- 
phyry as  an  island  or  reef  during  the  deposition  of  the  sandstone. 
These  facts  entirely  negative  the  view  that  these  hills  were  either 
ejected  as  an  igneous  mass,  or  thrust  up  as  such  by  upheaval.  They 
are  simply  projecting  points  of  an  eroded  formation. 


THE  QUAKTZ-PORPHYBY  OF  PlNE  BLUFF. 

Seventeen  miles  south  of  Berlin  there  rises  out  of  the  flood  plain 
of  the  Grand  river  a  conspicuous  mass  of  quartz-porphyry  known 
as  Pine  Bluff.  It  ascends  by  steep,  and  even  precipitous  acclivities 
to  a  height  of  one  hundred  feet,  and  being  entirely  isolated  from 
surrounding  elevations,  and  largely  bare  of  soil  and  vegetation,  be- 
comes a  striking  object.  The  rock  consists  of  white,  gray  and  flesh 
colored  crystals  of  orthoclase,  and  of  glassy  feldspar,  set  in  a  very 
hard,  gray  or  black  quartz-felsite  base.  The  crystals  of  feldspar  vary 
in  size  from  three-tenths  of  an  inch  in  length,  downwards,  but  are 
rendered  conspicuous  by  contrast  of  color.  The  rock  is  susceptible  of 
very  high  and  beautiful  polish,  but  is  wrought  with  difficulty  on  ac- 
count of  its  hardness.  The  dip  is  about  20°  to  the  E.  of  S.  Obscure 
glacial  striae,  still  preserved,  testify  to  its  endurance.  Their  direction 
is  S.  450  "W.  The  accompanying  profile  exhibits  its  relations  to  the 


A.RCHJEAN  FORMATIONS.  251 

Silurian  formations,  from  which  it  will  be  seen  that  it  rises  to  about 
the  base  of  the  Galena  limestone. 

FIG.  19. 


NORTH  AND  SOUTH  SECTION  THROUGH  PINE  BLUFF. 

1.   Quartz-Porphyry,  Pine  Bluff.     2.  Lower  Maguesian  limestone.    3.   Jit.  Peters  sandstone.    4. 
Trenton  limestone.    5.  Galena  limestone. 


TllE  QUARTZ-PORPHYKY  OF  MAKQUETTE. 

Near  Marquette,  a  little  more  than  twelve  miles  west  of  Pine  Bluff, 
very  similar  quartz- porphyries  display  themselves  in  more  considera- 
ble force,  constituting  a  group  of  prominent  hills.  A  portion  of  the 
rock  is  precisely  identical  in  character  with  that  of  Pine  Bluff,  and 
the  greater  mass  is  but  an  unimportant  variation  from  it,  but  cer- 
tain portions  depart  from  the  porphyritic  character,  and  become  al- 
most, or  entirely,  crypto-crystalline.  One  variety  of  this  kind  very 
closely  resembles  the  more  homogeneous  of  the  red  Huronian  quartz- 
ites,  and  another  is  a  compact  close-textured  rock,  usually  of  dark 
color,  but  sometimes  greenish.  Neither  of  these  varieties  occupies 
exclusively  any  one  horizon,  but  the  quartzite-like  variety  is  found  in 
the  more  southern  outcrops,  the  last  mentioned  kind  immediately 
north  of  that,  the  darker  porphyries  next,  and  the  coarser,  lighter 
colored  ones  in  the  most  northerly  exposures. 

The  bedding  is  very  obscure,  but  the  laminations  of  certain  portions 
and  belts  of  particular  varieties  of  rock  show  the  strike  to  be  north- 
eastward. The  dip  is  made  out  with  much  less  certainty,  but  ap- 
pears to  be  to  the  northward,  and  to  vary  from  1 5°  to  45°. 

Though  the  Berlin  porphyry  differs  from  that  of  Pine  Bluff  and  of 
Marquette  in  the  absence  of  glassy  feldspar,  yet  the  close  lithologi- 
cal  alliance  of  the  three  is  very  evident,  and  they  doubtless  all  belong 
to  the  same  group  of  the  Archaean  series.  The  general  strike  of 
these  formations,  projected  westward,  encounters  several  similar  out- 
liers, that  are  described  in  Prof.  Irving's  report,  and  still  further 
southwest  he  has  found  similar  quartz- porphyry  overlying  the  Bara- 
boo  quartzite.  There  seems  to  be  sufficient  reason  for  regarding  the 
latter  as  Huronian,  so  that  the  porphyries  must  be  regarded  as  a 
newer  portion  of  that  formation. 

All  of  these  masses  present  the  rounded  contour  of  glaciated  sur- 
faces, and  still  bear  the  glacial  groovings,  and,  in  some  cases  even 


252  GEOLOGY  OF  EASTERN  WISCONSIN. 

remnant  polished  spots,  and  from  all  these,  trains  of  porphyry  bowl- 
ders stretch  away  in  the  direction  of  the  striae. 


THE  QUARTZITES  OF  PORTLAND  AND  WATERLOO. 

Thirty-five  miles  south  of  Pine  Bluff,  over  an  area  entirely  covered 
by  Paleozoic  rocks,  some  as  recent  as  the  Galena,  we  again  encounter 
the  Archaean  rocks  in  the  form  of  the  quartzites  of  Portland  and 
"Waterloo. 

The  outcrops  in  the  town  of  Portland *  are  several  in  number.  The 
most  southwesterly  is  an  oval  island,  lying  mostly  in  the  S.  E.  qr.  of  Sec. 
33,  and  is  entirely  surrounded  by  lowland  or  marsh.  The  outcrop  at- 
tains but  a  slight  elevation,  and  its  rounded  contour  shows  abundant 
evidence  of  the  glacial  agencies  that  have  swept  over  it.  ]Srot  only 
striae,  but  deep,  broad  furrows,  show  the  direction  of  movement  to 
have  been  S.  15°  to  20°  W.  Bowlders  appear  in  great  force  upon  the 
protected  side  of  the  island,  and  doubtless  thickly  underlie  the  deep 
morass  in  that  direction,  as  they  appear  again  upon  the  hills  be- 
yond. Directly  to  the  east,  in  sec.  34,  there  is  a  slight  exposure  near 
the  base  of  a  somewhat  elevated  north  and  south  ridge,  of  which  it 
doubtless  forms  the  nucleus,  if  not  the  chief  portion. 

Less  than  one  mile  north  of  these  outcrops,  the  quartzite  again  dis- 
covers itself  on  the  brow  and  west  flank  of  the  ridge  facing  Waterloo 
Creek.  There  is  no  evidence  that  any  later  formation  overlies  the 
quartzite  between  this  and  the  two  preceding  outcrops,  and  so  the 
three  will  be  found  mapped  as  constituting  a  single  Archaean  area. 
A  short  distance  further  to  the  north  (N.  W.  qr.,  see.  27),  the  quartz- 
ite rises  in  the  midst  of  a  marsh-like  lake,  constituting  Rocky  Island. 
It  may  be  characterized  as  a  low  dome  covered  with  unsymmetrical 
roches  moutonees. 

About  two  miles  southeast,  at  the  foot  of  a  hill,  and  on  the  edge  of 
a  marsh,  occurs  a  low  and  limited  outcrop  (sec.  35,  S.  E.  J,  and  sec.  30, 
S.  W.  J).  One-half  mile  to  the  northeast,  across  a  marsh,  there  occurs 
another  exposure,  similarly  situated  in  the  southern  extremity  of  a 
north  and  south  ridge,  and  about  the  same  distance  to  the  southwest, 
still  another  one  may  be  seen ;  the  three  lying  nearly  in  a  straight 
line,  and  separated  by  marshes.  They  are  regarded  as  being  project- 
ing knobs  of  a  common  area,  and  are  so  mapped.  Between  these  and 
the  three  outcrops  first  mentioned,  as  also  between  both  these  and 

1  See  note  on  the  Age  of  the  Metamorphic  Rocks  of  Portland,  Dodge  Co.,  Wis.,  by 
R.  D.  Irving,  Am.  Jour.  Sci.,  Third  Series,  Vol.  V,  p.  282. 


ARCHJEAN  FORMATIONS.  253 

Rocky  Island,  later  formations  intervene,  so  that  they  must  be  regard- 
ed as  forming  three  distinct,  though  closely  associated,  surface  areas. 

The  first  mentioned  outlier  of  the  last  group  still  preserves  on  its 
exposed  surface  the  scorings  of  the  drift  forces,  there  being  two  sets, 
the  one  pointing  S.  33°  "W.,  and  the  other  S.  55°  W. 

From  the  several  outliers  there  stretch  away  to  the  southwestward 
trains  of  bowlders  of  quartzite,  which  gradually  spread  out  into  a  fan- 
like  form,  the  fragments  meanwhile  becoming  more  rounded,  smaller, 
and  scattered.  I  have  traced  them  fifty  miles  distant  into  Illinois. 
A  figure  illustrating  these  facts  has  already  been  given.  Their  special 
significance  here  relates  to  the  question  whether  other  masses  of 
quartzite  protrude  through  the  Paleozoic  formations  in  this  region. 
If  so,  they  should  indicate  their  presence  by  erratics  in  the  drift. 
Bowlders,  in  limited  numbers,  reach  about  three  miles  east,  and  a 
somewhat  greater  distance  north  of  the  outcrops,  but  as  traced  in 
those  directions,  no  concentration  toward  a  point  of  origin  was  ob- 
served with  sufficient  definiteness  to  locate  their  source. 

The  discovery  of  a  train  in  the  town  of  Waterloo  led  to  more  sat- 
isfactory results.  The  abundance  of  angular  blocks  in  the  drift  led 
to  the  conviction  that  their  source  was  in  the  immediate  neighbor- 
hood, and,  under  the  guidance  of  the  Rev.  Gr.  S.  Hubbs,  the  actual 
outcrop  was  found.  Like  the  others,  it  lies  at  the  foot  of  a  ridge  on 
the  border  of  a  marsh.  The  exposure  is  small,  but  interesting. 

At  one  point  there  is  a  very  fine  exhibition  of  ripple  marks  running 
parallel  to  the  dip,  thus  demonstrating  the  true 
tilting  with  certainty.  This  was  found  to  be 

E.,  the  strike  being  K  45°  W. 
The  rock  of  all  these  outcrops  is  a  hard, 
OUTLIER,  thoroughly  metamorphosed  red,  or  gray  quartz- 
Town  of  Waterloo.  jte>  Metamorphic  conglomerates  occur  in  cer- 
tain portions:  In  others  there  is  a  foliated  material  of  talcose  appear- 
ance, yet  seldom  sufficient  to  give  the  rock  a  schistose  structure.  The 
gray  variety  of  quartzite  predominates,  especially  in  the  more  westerly 
outliers,  while  the  red  is  more  abundant  in  the  eastern. 

The  relations  of  these  quartzites  to  the  surrounding  formations  are 
exceedingly  interesting.  About  eighty  rods  south  of  the  outlier  in 
Waterloo,  the  lower  layers  of  the  Trenton  limestone,  reposing  upon 
the  St.  Peters  sandstone,  occur  at  the  same  level  as  the  quartzite,  with 
no  indication  of  disturbance.  The  accompanying  figure  will  render 
the  situation  clear. 

In  the  intermediate  space  are  bowlders  of  conglomerate,  the  peb- 
bles of  which  are  of  quartzite,  precisely  similar  to  that  of  the  out- 


254  GEOLOGY  OF  EASTERN  WISCONSIN. 

liers,  while  the  matrix  is  of  white  sand  similar  to  that  of  the  St. 
Peters  sandstone.  There  are  also  fragments  of  sandstone  contain- 
ing the  cylindrical  cavities  known  as  Scolithus.  A  single  bowlder 
was  also  found  uniting  the  two.  I  have  found  Scholithus  tubes  in 
the  upper  transition  layers  of  the  St.  Peters  sandstone,  and  as  there  is 
no  known  Potsdam  sandstone  along  the  line  of  drift  for  more  than 
one  hundred  miles,  and  rarely  then,  in  contact  with  quartzite,  it  seems 
altogether  most  rational  to  conclude  that  the  St.  Peters  sandstone 
was  laid  down  around  the  island  of  quartzite  from  which  the  pebbles 

FIG.  21. 

* 80  Hotfs 


PROFILE  SECTION  SHOWING  THE  RELATIONS  OF  THE  WATERLOO  QUARTZITE. 
1.  Quartzite.    2.  St.  Peters  Sandstone.    3.  Trenton  Limestone. 

of  the  conglomerate  were  derived  by  beach  action,  and  that  the 
bowlders  in  question  were  derived  from  the  deposit  thus  formed.  The 
greater  fineness  of  the  rock,  which  is  a  matter  of  observation,  may 
account  for  the  preservation  of  the  Scolithus  tubes,  which  are  very 
rare  in  the  more  friable  portions.  This  view  is  both  corroborated  and 
complicated  by  the  still  more  interesting  facts  observed  in  the  town  of 
Portland.  Opposite  Rock  Island  and  near  the  water's  edge,  we  find  a 
white  sandstone  bearing  abundant  well  preserved  Scolithus  tubes. 
This  graduates  above  into  a  fine  conglomerate,  which  becomes  coarser 
and  coarser  until  at  a  height  of  48  feet,  where  it  adjoins  the  quartzite, 
it  consists  of  bowlders  three  or  four  feet  in  diameter,  imbedded  in. 
finer  grades  of  conglomerate.  There  is  here  no  question  as  to  the  ori- 
gin of  the  conglomerate,  or  of  the  relations  of  the  Scolithus  to  it. 
The  quartzite  rose  as  a  rocky  island  in  the  depositing  seas,  and  yield- 
ed its  material  to  the  beating  of  the  waves,  by  which  the  conglomerate 
was  formed. 

But  on  the  opposite  side  of  the  ridge,  somewhat  more  than  a  mile 
distant,  a  peculiar  shaly,  arenaceous  rock  is  found  at  the  same  eleva- 
tion. One  variety  of  this  rock  is  exposed  in  the  railroad  cut  in  Sec. 
3  of  the  town  of  Waterloo.  It  is  of  variegated,  reddish  aspect  and 
irregular  texture,  and  closely  resembles  the  variegated  shales  of  the 
Mendota  beds  of  the  Potsdam,  and  also  some  of  the  modified  forms  of 
the  St.  Peters  sandstone,  where  it  lies  contiguous  to  the  domes  of- 
Lower  Magnesian  limestone,  subsequently  to  be  described.  It  has 
been  penetrated  at  several  points  in  the  vicinity  by  wells  which  in 
some  cases  reach  the  quartzite  underneath  it.  The  owners  of  the 
wells  usually  describe  it  as  a  red,  sandy  rock.  At  one  point  (middle 


ARCILEAN  FORMATIONS. 


255 


N".  line  of  K.  E.  qr.  of  S.  W.  qr.,  Sec.  35,  Portland),  a  rock  of  similar 
nature,  but  of  light  buff  color,  was  penetrated  to  a  depth  of  18  feet, 
below  36  feet  of  drift,  when  quartzite  was  reached.  In  the  S.  E.  qr. 
of  Sec.  3,  town  of  Waterloo,  after  18  feet  of  drift,  41  feet  of  what 
was  described  as  a  rather  soft,  sandy  red  rock,  was  penetrated,  below 
which  a  hard  rock,  probably  quartzite,  was  found.  The  accompany- 
ing cut  shows  the  relations  of  this  rock  with  the  quartzite  and  con- 
glomerate. 

FIG.  22. 


NORTH  AND  SOUTH  SECTION  THROUGH  PORTLAND  QUABTZITE. 
1.  Quartzite.    2.  Conglomerate.    3.  Shaly  Sandrock. 

Figure  23  shows  the  horizon  which  the  quartzite  and  the  accompa- 
nying formations  occupy.  The  nearest  approach  of  the  Trenton  and 
St.  Peters,  in  their  normal  character,  is  about  two  miles. 

FIG.  23. 


PROFILE  SECTION,  SHOWING  THE  RELATIONS  OF  THE  PORTLAND  QUAHTZITK. 
1.  Quartzite.    2.  Shaly  Sandrock.    3.  Lower  Magnesian  Limestone.    4.  St.  Peters  Sandstone.    5. 

Trenton  Limestone. 

"Without  assuming  demonstration,  it  seems  most  in  harmony  with 
all  the  facts,  and  freest  from  gratuitous  assumptions  to  refer  the 
conglomerates,  sandstones  and  shaly  sandrock  to  the  period  of  the 
St.  Peters,  and  they  will  be  found  so  mapped.1  It  is  to  be  remarked 
(1)  That  these  quartzites  were  originally  sandstones  and  conglomer- 
ates. (2)  That  they  were  metamorphosed  before  the  deposit  of  the 
neighboring  horizontal  rocks,  since  the  pebbles  included  in  the  latter 
are  metamorphic.  (3)  That  they  were  tilted  before  the  deposit  of 
horizontal  rocks,  as  shown  by  their  unconformability.  (4)  That  their 
upheaval  and  metamorphism  were  probably  synchronous  and  congen- 
ite.  (5)  That  extensive  erosion  took  place  before  they  were  com- 
pletely covered  and  protected,  as  shown  by  the  fact  that  they  expose 

4  On  the  accompanying  map  the  area  of  quartzite  in  Sec.  34  is  placed  one-third  mile 
too  far  north. 


256  GEOLOGY  OF  EASTERN  WISCONSIN. 

in  great  thickness  their  truncated  edges  and  dip  at  a  high  angle  in  a 
common  direction  —  northeast.  (6)  That  there  was  a  vast  lapse  of 
time  in  which  the  erosion  might  take  place.  These  rocks  are  un- 
doubtedly a  portion  of  the  Baraboo  quartzite  series  which  has  been 
proven  to  be  pre-Potsdam,  and  since  the  Portland  and  Waterloo 
quartzites  rise  at  their  highest  points  into  the  Trenton  horizon,  there 
must  at  least  have  elapsed  time  enough  for  the  deposit  of  1,200  feet 
of  sandstone  and  limestone  before  they  were  finally  covered  in  the 
Trenton  period. 


POTSDAM  SANDSTONE.  357 


OHAPTEE  VII. 

LOWER  SILURIAK 

POTSDAM  SANDSTONE. 

There  rests  upon  the  very  irregular  surface  of  the  metamorphic 
rocks  above  described,  filling  up  its  depressions  and  for  the  most 
part  surmounting  its  hills  (over  the  area  so  occupied),  a  deep  and  ex- 
tensive deposit  of  sandstone,  known  under  the  above  name.  That  it 
is  the  exact  equivalent  of  the  Potsdam  sandstone  of  JS"ew  York,  as 
would  seem  to  be  implied  by  the  name,  is  not  absolutely  certain,  but 
as  the  term  has  been  used  to  designate  this  formation  in  previous  re- 
ports upon  the  geology  of  the  state,  and  as  the  weight  of  evidence 
and  authority  favors  this  view,  the  name  Potsdam  sandstone  will  be 
used  without  further  qualification  in  this  report. 

The  upper  surface  of  this  formation  is  essentially  uniform  and 
nearly  horizontal,  and  is  overlaid  by  the  Lower  Magnesian  limestone. 
These  two  formations,  then,  the  limestone  above  and  the  Archaean 
rocks  below,  furnish  one  of  the  means  by  which  the  sandstone  may 
be  identified  and  its  position  and  thickness  determined.  Since  its 
upper  surface  is  nearly  uniform,  and  its  bed  very  irregular,  it 
necessarily  varies  greatly  in  thickness,  the  known  range  within 
the  state  being  from  zero  to  about  1,000  feet.  Within  our  district 
its  variation  in  thickness  is  known  to  be  but  little  short  of  this,  and 
from  the  nature  of  the  case,  it  is  evident  that  the  extreme  thickness 
of  this  rock  may  much  exceed  that  which  has  been  observed.  This 
irregularity  in  thickness-  should  be  kept  in  mind  in  making  any  cal- 
culations dependent  upon  the  depth  of  this  formation. 

General  Character.  The  rock  is  chiefly  composed  of  cemented 
grains  of  silicious  sand.  To  the  unassisted  eye,  these  grains  appear 
spherical,  but  upon  examination  under  the  microscope,  they  are  seen 
to  be  more  or  less  angular  and  irregular,  and  show  that  they  have 
been  formed  from  small  fragments,  and  in  some  cases,  perhaps, 
minute  crystals  of  quartz,  which  have  been  worn  by  friction  to  their 
present  form.  These  grains  vary  much  in  size  in  different  localities, 
and  in  the  various  strata  of  the  formation. 
Wis.  Sun.— 17 


258  GEOLOGY  OF  EASTERN  WISCONSIN. 

In  general,  as  seen  in  outcrops  in  eastern  Wisconsin,  they  are 
neither  very  coarse  nor  very  fine,  but  range  through  the  medium 
varieties.  Near  the  base  of  the  formation  a  very  coarse  grained 
sandstone  occurs,  but  it  is  not  known  to  outcrop  in  the  district.  In 
some  cases  these  grains  are  embedded  in  more  finely  comminuted 
silicious  powder,  doubtless  worn  from  the  grains  themselves,  so  that 
the  rock  possesses  considerable  compactness,  but  only  a  small  degree 
of  cohesive  power.  In  other  cases,  the  filling  between  the  grains  is  a 
clayey  material,  or  a  green  earth,  forming  an  argillaceous  sandstone, 
or  one  of  the  varieties  of  greensand. 

Still  again,  and  very  commonly,  the  grains  of  sand  are  firmly  ce- 
mented by  calcareous  or  ferruginous  matter.  In  many  cases  this  is 
not  so  much  a  filling  of  the  spaces  between  the  grains  as  it  is  a  coat- 
ing of  the  grains  themselves,  by  which  they  are  firmly  bound  to- 
gether. It  is  this  variety  that  furnishes  the  most  serviceable  building 
material. 

As  a  result  of  these  facts,  the  formation  presents  several  varieties 
of  sandstone,  which  may  be  known  respectively  as  the  calcareous,  the 
non-calcareous,  the  argillaceous,  the  ferruginous,  and  the  green  sand. 
Sandstone  entirely  free  from  calcareous  matter  is  rare  in  this  forma- 
tion in  eastern  Wisconsin. 

Whether  we  examine  outcropping  ledges,  artificial  exposures,  or  the 
drillings  of  Artesian  wells,  the  presence  of  more  or  less  of  lime  is 
usually  indicated,  except  in  the  lowest  stratum  of  the  formation.  As 
has  been  before  remarked,  the  waters  issuing  from  this  formation 
usually  contain  a  small  percentage  of  lime  salts.  Whether  they  de- 
rive their  calcareous  burden  from  the  sandstone,  or,  on  the  contrary, 
are  the  sources  in  part  of  the  lime  in  it,  having  obtained  it  originally 
from  the  limestone  above  and  yielded  it  to  the  sandstone  in  passing 
through  it,  may  be  a  matter  of  doubt,  in  some  cases,  but  a  portion  of 
the  lime  was  undoubtedly  deposited  at  the  same  time  with  the  sand. 

All  of  the  non-calcareous  sandstones,  observed  in  the  district 
under  consideration,  crumble  so  easily  as  to  be  of  little  industrial 
importance  except  as  a  source  of  sand,  and  as  they  form  a  sterile  soil, 
their  rarity  may  be  considered  a  matter  of  good  fortune. 

In  the  argillaceous  class,  the  clayey  material  sometimes  becomes 
so  abundant  as  to  render  the  rock  shaly,  and  in  some  cases  it  so  far 
predominates  that  the  rock  is  known  as  a  shale,  rather  than  a  sand- 
stone. These  argillaceous  layers  are  usually  impervious  to  water, 
and  demonstrate  their  utility  by  giving  origin  to  valuable  springs. 

There  are  two  classes  of  green  sand,  one,  which  consists  of  grains 
of  quartz  colored  by  some  substance  —  iron  in  those  cases  which  I 


POTSDAM  SANDSTONE.  259 

have  examined  —  the  other  and  much  more  prevalent,  which  consists 
of  a  mixture  of  ordinary  white  quartz  grains,  and  deep-green  grains 
of  glauconite,  or  a  closely  allied  mineral. 

The  ferruginous  varieties  embrace  at  one  extreme,  those  in  which 
the  amount  of  iron  oxide  is  barely  sufficient  to  color  or  cement  the 
mass,  and  at  the  other,  those  in  which  it  becomes  so  great  as  to  justi- 
fy calling  the  mass  an  iron  ore.  Neither  of  these  classes  is  abun- 
dant in  this  portion  of  the  state,  though  important  features  in  other 
parts.  The  sandstone  of  this  region  is  usually  very  light  colored,  and 
nodules,  seams,  or  layers  of  iron,  though  present,  attain  to  no  signifi- 
cant development. 

As  has  been  already  remarked,  the  great  mass  of  this  sandstone  is 
more  or  less  calcareous.  The  limy  portions  become  so  great  in  some 
layers  that  they  are  more  properly  limestones  than  sandstones.  The 
lime  in  this  case,  as  is  usual  in  this  state,  is  associated  with  mag- 
nesia, so  that  these  layers  become  really  arenaceous  dolomites.  In 
some  portions,  the  calcareous  matter,  instead  of  being  dissemina- 
ted through  the  rock,  forms  concretions,  by  binding  lumps  of  sand 
into  hard  spherical  masses,  giving  the  beds  a  nodular  structure. 

The  foregoing  general  statements  may  perhaps  suffice  to  indicate 
the  prevailing  chemical  and  molecular  nature,  and  the  minute  struc- 
ture of  this  formation.  More  specific  facts  will  be  found  in  connec- 
tion with  the  local  sections  and  descriptions.  We  may  now  consider 
its  more  massive  characters.  Where  bedding  is  distinctly  marked 
the  layers  are  not  usually  more  than  three  or  four  feet  in  thickness. 
From  this  thickness  they  are  to  be  found  of  all  lower  dimensions  down 
to  layers  of  slate-like  thinness.  The  beds  show  oblique  lamination, 
ripple  marks,  and  other  evidences  of.  shallow  water  deposit. 

Owing  to  the  prevalence  of  heavy  deposits  of  drift,  exposures  of 
this  formation  in  eastern  Wisconsin  are  quite  unfrequent,  and  very 
limited  in  extent;  a  very  fortunate  circumstance  for  the  agriculturist, 
though  quite  the  reverse  for  the  geologist.  However,  by  diligent 
search  and  careful  collating  of  data,  it  appears  that  the  formation 
consists  of  six  subdivisions,  as  follows,  beginning  at  the  top: 

Sandstone  (Madison) 35  feet. 

Limestone,  shale  and  sandstone  (Mendota) , .     60     " 

Sandstone,  calcareous 155     " 

Bluish  shale,  calcareous, 80     " 

Sandstone,  slightly  calcareous, 160     " 

Very  coarse  sandstone,  non-calcareous, 280     " 

The  thicknesses  given  are  subject  to  considerable  variation.  As  a 
general  rule  they  grow  less  toward  the  northeast.  Where  the  total 


260  GEOLOGY  OF  EASTERN  WISCONSIN. 

thickness  of  the  formation  is  reduced  by  the  inequalities  of  its  Arch- 
aean bottom,  it  is  by  the  loss  of  the  lower  members  of  the  group  and 
not  by  the  thinning  of  all. 

/.  Madison  Sandstone.  This  name  has  been  assigned,  by  Prof. 
Irving,  to  the  uppermost  subdivision,  from  its  occurrence  in  the  vi- 
cinity of  the  capital,  where  it  is  extensively  used,  under  that  name,  as 
a  building  stone.  He  regards  this  as  a  member  of  the  Calciferous 
group  above,  rather  than  of  the  Potsdam,  in  respect  to  which,  howev- 
er, I  feel  compelled  to  differ  from  him,  for  reasons  given  below. 

At  its  more  typical  localities,  this  sandstone  is  a  rather  coarse 
grained,  thick  bedded,  compact,  but  soft,  slightly  calcareous,  light 
colored  sandstone.  It  is  best  shown  at  Lucas  Point,  on  the  southern 
shore  of  Green  Lake,  a  few  miles  west  of  Ripon,  where,  however  it  is 
more  than  usually  fine-grained. 

At  this  point  it  is  horizontally  laminated,  and  marked  by  wavy 
lines  of  reddish  yellow  iron  stains,  though  these  are  probably  not  con- 
stant characters.  In  its  upper  portion,  immediately  beneath  the  low- 
er magnesian  limestone,  it  is  at  most  locations  coarse,  and  the  topmost 
layer  is  of  ten  broken  up  and  mixed  with  calcareous  material,  giving  it 
a  coarsely  brecciated  structure.  This  layer,  or  its  equivalent,  usually 
marks  the  upper  limit  of  the  formation  with  distinctness,  though  more 
or  less  of  sand  mingles  with  the  lower  ledges  of  the  limestone  above. 

2.  Mendota  Limestone.  This  name  has  been  given  to  this  group  of 
strata,  by  Prof.  Irving,  from  its  occurrence  on  Lake  Mendota,  near 
Madison.  The  term  limestone  is  applicable,  however,  to  this  division 
in  eastern  Wisconsin,  only  in  a  qualified  sense.  It  consists  really  of  a 
group  of  alternating  strata  of  arenaceous  magnesian  limestone,  sandy 
calcareous  shales,  and  shaly  and  calcareous  sandstones.  The  lime- 
stones are  soft,  granular,  porous,  friable,  rather  thin  bedded,  buff 
colored,  and  frequently  contain  searns  of  greensand. 

They  resist  erosion  to  a  greater  degree  than  the  sandstones  above 
and  below,  and  so  sometimes  form  the  protecting  cap  of  terraces. 

The  shales  are  variegated  with  yellow,  red  and  purple.  Those  of  the 
latter  class  are  quite  characteristic,  though  something  very  similar 
occurs  at  a  few  exceptional  localities  in  the  St.  Peters  sandstone. 
The  purple  portion,  which  only  makes  up  a  part  of  the  mass  of  the 
rock,  consists  of  irregular  layers,  lumps  and  patches  mixed  with  red- 
dish and  yellowish  portions,  giving  the  whole  a  peculiar  mottled  ap- 
pearance. The  lighter  colored  shales  occur  intimately  associated  with 
these.  Both  classes  are  more  or  less  arenaceous  and  calcareous,  are 
soft  and  brittle,  easily  crushed,  and  readily  decomposed  under  the  ac- 
tion of  atmospheric  agencies. 


POTSDAM  SANDSTONE.  261 

The  sandstones  are  of  two  kinds,  those  consisting  of  the  common 
white,  buff,  yellow  or  orange  quartzose  sand,  with  more  or  less  of  cal- 
careous and  aluminous  admixture,  and  those  formed  by  a  mingling  of 
the  common  quartzose  sand  with  green  particles  of  glauconite,  and 
altered  forms  of  it,  producing  as  a  result  various  shades  of  gray,  yel- 
low, green  and  mottled  sandstones.  The  component  grains  frequently 
have  but  a  slight  cohesion,  so  that  the  mass  is  fittingly  termed  green 
sand. 

The  upper  and  lower  limits  of  the  Mendota  group  are  scarcely  de- 
finable. It  graduates  above  into  the  Madison  sandstone,  so  as  to  make 
it  difficult  to  draw  a  line  between  the  two,  and  below,  the  alternation 
of  calcareous  and  arenaceous  rock  make  it  equally  difficult  to  say 
where  the  series  ends. 

A  thickness  of  fifteen  or  twenty  feet  would  include  the  greater  por- 
tion of  the  lime  rock,  while  about  sixty  feet  would  be  required  to 
cover  the  entire  alternating  series.  This  will  be  clearly  seen  by  in- 
specting the  local  sections  subsequently  given. 

This  constitutes  one  of  the  objections  to  separating  this  from  the 
Potsdam  sandstone  series,  and  grouping  it  with  the  Lower  Magnesian 
series.  The  lower  limit  of  the  Magnesian  limestone  is  in  this  region, 
and  elsewhere  so  far  as  I  have  personally  observed,  well  defined,  al- 
though sandstone  mingles  with  the  formation  above  and  calcareous 
strata  extend  scores,  if  not  hundreds,  of  feet  below  into  the  Potsdam 
sandstone.  Aside  from  other  objections,  there  seems  to  me  no  good 
reason  for  placing  the  dividing  horizon  at  any  other  point  than  that 
which  has  very  generally  been  recognized  by  geologists,  viz. :  at  the 
top  of  the  Madison  beds. 

It  is  to  be  remarked,  however,  that  in  central  Wisconsin  where  the 
Mendota  beds  develop  a  greater  thickness  and  purity  of  dolomitic 
character  as  well  as  greater  lithological  similarity  to  the  Lower  Mag- 
nesian limestone,  they  have  heretofore  been  mistaken  for  that  forma- 
tion, and  something  of  confusion  introduced  into  the  geology  of  this 
horizon,  which  the  distinct  recognition  of  the  Mendota  beds  by  Prof. 
Irving  has  removed. 

The  paleo'iitolofjical  evidence  very  strongly  corroborates  the  view 
here  taken.  "Without  attempting  an  exhaustive  discussion,  it  may  be 
remarked  that  the  Mendota  beds  are  undoubtedly  the  eastern  equiv- 
alents of  Dr.  Owen's  Fifth  Trilobite  bed,  the  common  horizon  being 
characterized  by  the  presence  of  Dicellocephalus  Jtfinnesotensis,  D. 
Pepinensis,  Lingula  aurora,  L.  mosia,  and  a  few  other  species  of  lim- 
ited horizontal  distribution.  The  primordial  aspect  of  this  fauna  is 
unquestionable.  The  collections  of  this  season  have  shown  Lingula 


262  GEOLOGY  OF  EASTERN  WISCONSIN. 

mosia  to  be  associated  with  Lingulepis  pinniformis,  which  is  con- 
sidered by  Owen  and  Hall  as  characterizing  the  lower  beds  of  the  Pots- 
dam, and  Dicellocephalus  Pepin  ens-is  was  found  with  Illaenurus 
quadrettus,  which  Prof.  Hall  refers  to  the  middle  Potsdam,  thus  show- 
ing specific  paleontological  bonds  with  the  lower  strata. 

On  the  other  hand  there  is  not,  so  far  as  I  am  aware,  any  case  of 
the  occurrence  of  any  of  these  species  in  the  Lower  Magnesian  lime- 
stone, as  limited  in  this  report,  there  being  ample  reasons  for  believ- 
ing that  in  all  cases  where  Dicellocephalus  Minnesotensis  has  been 
doubtfully  referred  to  this  horizon,  the  specimens  really  belonged  to 
the  Mendota  or  other  intercalated  beds. 

The  lower  divisions,  constituting  the  main  body  of  the  Potsdam 
sandstone,  present  but  very  few  exposures  in  this  region,  and  these  of 
very  limited  extent,  so  that  we  are  dependent  chiefly  on  the  evidence 
derived  from  Artesian  wells  for  positive  knowledge  of  their  nature. 
So  far  as  thus  indicated,  there  are  four  subdivisions. 

j.  That  which  lies  next  below  the  Mendota  beds  is  a  light  colored, 
fine  to  medium  grained  sandstone.  The  constituent  grains  are  chiefly 
quartz,  with  a  less  quantity  of  chert  and  a  few  limestone  and  granitic 
particles  in  some  portions.  It  is  slightly  calcareous,  even  where  the 
limestone  particles  are  not  observable. 

4.  The  next  division  consists  of  a  bluish  green  shale  of  highly  cal- 
careous nature,  containing  minute,  glistening,  mica-like  scales.     It 
was  not  seen  in  outcrop,  and  may  be  quite  local,  though  it  appears 
to  be  represented  in  the  northwestern  part  of  the  state. 

5.  The  fifth  division  is  very  similar  in  nature  to  that  above  the  last, 
being  a  rather  fine  grained,  light  colored  quartzose  sandstone,  contain- 
ing occasionally  some  clay-like  calcareous  matter. 

6.  The  lowest  subdivision  is  a  very  coarse,  non-calcareous  sand- 
stone, composed  of  large  grains  of  transparent,  light  colored  quartz  of 
irregular  but  rounded  form. 

Organic  IZemains.  The  following  is  a  list  of  the  fossils  found  in 
the  Potsdam  in  this  portion  of  the  state.  These,  and  all  subsequent 
identifications  in  this  report  were  made  by  Prof.  R.  P.  Whitfield, 
•whose  eminent  qualifications  are  a  guaranty  of  their  correctness: 

PLANTS. 
Paleophycus.     Sp.  und. 

MOLLUSCA.  —  BRACHIOPODA. 
Orthis  Pepina. 

AETICULATA.  —  ANNELIDA. 
Tubes  of  scolithus? 


POTSDAM  SANDSTONE.  263 

TKILOBITES. 

Conocephalites  diadematus,  H. 
Conocephalites  minor,  Slium. 
Conocephalites  Gibbsi,  n.  sp.1 
Dicellocephalus  Misa,  H. 

This  is  probably  very  far  from  being  a  fair  representation  of  the 
actual  fauna,  but  the  meagerness  of  the  outcrops  in  this  region,  and 
the  fact  that  the  rock  is  very  rarely  quarried,  make  it  practically 
impossible  to  secure  a  full  collection. 

Method  of  Deposit.  That  this  sandstone  was  deposited  beneath 
the  ocean  is  shown  by  the  remains  of  marine  life  found  in  it.  That 
the  water  was  comparatively  shallow  is  indicated  by  the  ripple  marks 
and  beach  structure  that  abound  in  the  formation.  The  rounded  and 
yet  irregular  character  of  the  grains  of  sand  that  constitute  the  chief 
element  of  the  rock  leaves  no  doubt  that  they  were  originally  small, 
angular  grains  of  quartz  that  have  been  worn  by  friction  to  their 
present  form.  The  fact  that  this  formation  lies  upon  the  surface  of 
the  Archaean  rocks,  which  abound  in  quartz  in  the  form  of  irregular 
grains  and  crystals,  and  in  mica,  feldspar  and  other  minerals  found 
in  the  sandstone,  that  these  rocks  have  been  decomposed  and  eroded 
to  an  enormous  extent,  and  that  they  were,  at  the  time  this  deposi- 
tion was  in  progress,  exposed  to  the  action  of  the  waves  and  atmo- 
spheric influences,  make  it  certain  that  the  sandstone  was  derived 
from  these  older  rocks,  and  that  this  was  accomplished  by  the  same 
process  of  wear,  decay,  and  redeposit  that  is  in  action  at  the  present 
time,  producing  similar  accumulations  of  sand,  that  may  in  time  be- 
come hardened  to  rock.  The  clayey  material  was  doubtless  derived 
in  the  same  way  from  the  feldspar  and  other  aluminous  ingredients 
of  the  same  granitic  rocks,  but  the  calcareous  portion  was  doubtless 
chiefly  formed  through  the  agency  of  marine  life. 

A  microscopic  examination  of  the  grains  of  sand  is  entirely  fatal 
to  the  view  still  occasionally  advanced,  that  they  were  produced  by 
crystalization  from  solution,  as  they  neither  have  in  general  the  crys- 
talline nor  concretionary  form,  nor  one  that  would  naturally  be  de- 
rived from  either  of  these  by  friction,  if  indeed  friction  were  suppos- 
able  under  that  theory. 

Extent.     It  has  heretofore  been  remarked  that  the  Potsdam  sand- 

1  The  names  of  new  species  given  in  this  volume  are  from  the  manuscript  of  Prof. 
Whitfiekl,  which  will  be  published  at  an  early  day.  They  are  here  introduced  for  the 
obvious  value  they  will  give  the  report  when  the  descriptions  shall  be  published,  and 
with  no  reference  to  any  claim  to  priority  of  publication. 


264:  GEOLOGY  OP  EASTERN  WISCONSIN. 

stone  in  Wisconsin  has  the  general  form  of  a  crescent.  "We  have  the 
right  or  eastern  horn  of  this  crescent  under  consideration.  It  enters 
the  district  obliquely  from  the  southwest,  and  occupies  the  western 
margin  of  Green  Lake,  Winnebago  and  Outagamie  counties,  from 
whence  it  extends  to  the  northeastward,  passing  into  Michigan  across 
the  upper  great  bend  in  the  Menomonee  river.  It  is  much  narrower 
in  this  than  in  the  central  portion  of  the  state,  averaging  only  from 
ten  to  fifteen  miles  in  width.  The  formations  in  this  part  of  the 
state  have  a  rudely  zigzag  or  stair-like  outline,  in  which  this  sand- 
stone participates.  This  is  more  especially  true  of  its  upper  limit  or 
eastern  boundary,  where  it  is  overlaid  by  the  Lower  Magnesian  lime- 
stone. Its  lower  limit  cannot  be  mapped  with  equal  precision,  owing 
to  the  unevenness  of  the  underlying  formation  and  the  ever  present 
obscuring  drift  accumulations.  Beyond  the  limits  marked  on  the 
maps,,  where  detailed  investigations  have  not  yet  been  made,  isolated 
patches  will  doubtless  be  found  resting  upon  the  Archaean  rocks. 

A  more  clear  and  accurate  view  of  the  surface  extent  and  location 
of  this  rock  than  it  is  possible  to  convey  by  verbal  description,  may 
be  obtained  by  consulting  the  accompanying  maps,  to  which  the  at- 
tention of  the  reader  is  respectfully  invited. 

The  formation  dips  to  the  east,  and  passes  under  all  the  formations 
lying  in  that  direction,  as  shown  in  the  sections  on  the  accompanying 
maps,  and  in  this  volume  under  the  head  of  Artesian  "Wells,  so  that 
it  underlies  at  varying  but  ascertainable  depths  the  whole  of  the  east- 
ern part  of  the  state. 

SECTIONS  AND  LOCAL  DESCRIPTIONS. 

The  township  of  Kingston  in  the  southwest  corner  of  Green  Lake  county,  being-  the 
most  southerly  town  in  the  district  under  consideration  that  is  occupied  to  any  extent 
by  this  formation  may  serve  us  as  a  suitable  point  whence  to  proceed  northward  in  sketch- 
big  such  local  developments  of  this  formation  as  may  seem  to  demand  notice,  the  more 
fittingly  so  because  it  presents  several  prominent  elevations  that  expose  the  formation. 
The  most  satisfactory  of  these  is  Bartholomew's  Bluff,  in  sec.  15,  S.  hf  of  N.  E.  qr.,  T. 
14,  R.  11  E.  This  hill  is  conspicuously  terraced,  the  lower  shelf  being  capped  by  the 
Mendota  beds  and  the  upper  by  the  more  enduring  Lower  Magnesian  limestone.  The 
sandstones  that  form  the  rest  of  the  hill,  being  soft,  have  been  more  affected  by  erod- 
ing agencies,  leaving  limestone-capped  benches  as  seen  in  the  accompanying  figure. 

The  following  is  the  section  exposed  at  this  point,  in  descending  order: 

1.  Bluish- gray,  thick  bedded,  sub-crystalline,  slightly  silicious  dolomite,  uneven  tex- 
ture, granular  in  part,  compact  in  part,  and  approaching  a  brecciated  structure  in  por- 
tions, weathering  to  a  rough  ragged  aspect;  fossils  absent  or  very  rare;  the  bottom  lay- 
ers of  the  Lower  Magnesian  limestone,  not  completely  exposed  but  probably  about  20 
feet  in  thickness. 

2.  Slope  of  the  terrace,  concealed  by  debris;  known  to  be  occupied  in  part  at  least  by 
a  yellowish  quartzose  sandstone,  with  slight  calcareous  cement.    It  is  probable,  from  ob- 


POTSDAM  SANDSTONE. 


265 


Fig.  24. 


servations  elsewhere,  that  the  whole  slope  is  underlaid  by  the  Madison  sandstone.   Thick- 
ness 30  feet. 

3    Rotten  calcareous  chipstone,  occupying  the  surface  of  the  lower  terrace,  derived  by 

disintegration  from  a  rock  similar  in  char- 
acter to  the  stratum  below.  Thickness  3 
feet. 

4.  Light  butt',  thin  bedded,  impure,  gran- 
ular, porous,  soft,  easily  fractured  magne- 
sian  limestone,  marked  with  fucoidal  impres- 
sions and  interlaid  with  thin  seams  of  green 
sand.    Examined  under  the  microscope,  the 
component  grains  appear  very  angular  and 
in  the  dry  state  mostly  opaque.    On  the  addi- 
tion of  acid,  part  are  dissolved  with  efferves- 
cence,   leaving  many  transparent  angular 
particles  insoluble  in  warm  acid.    Used  for 
building  purposes.    Thickness  8  feet. 

5.  Unexposed,  4  feet. 

6.  Greenish  and  grayish,   scarcely  cohe- 
rent sandstone,  composed  of  white  or  light 
colored  grains  of  quartzose  sand  and  green 
grains  of  glauconite.    Thickness  6  feet. 

7.  Calcareous,  banded  and  mottled  white 
and  orange,  coarse  granular,  sandrock,  part- 
ly formed  of   quartz  grains  and  partly  of 
small  crystals  of  dolomite.     Thickness,  5% 
inches. 

8.  Soft,  white,  very  friable,  quartzose  sandstone.    Thickness,  2  feet  and  5  inches. 

9.  Calcareous  layer  of  mottled,  greenish  and  orange  color,  coarse  granular,  uneven 
texture  and  medium  hardness,  graduating  into  the  green  sand  below.    Thickness,  9 
inches. 

10.  Green  sand  of  deep  color,  speckled"  with  reddish  iron  stains,  very  friable,  gradu- 
ating into  the  layer  above.    Thickness,  21  inches. 

11.  Porous,  granular,  crystalline  dolomitic  layers,  marked  by  nodules  of  hematite. 
One  layer  is  7%  inches  thick,  and  firm  and  excellent  for  building  purposes.    The  layers 
are  separated  by  thin  seams  of  green  sand.    Thickness,  3  feet  and  6  inches. 

12.  Greenish  white  sandstone  containing  spherical  concretions  and  Scolithus  tubes. 
The  walls  of  the  tubes  are  usually  cemented  with  iron  oxide  and  the  fossil  stands  out 
beautifully  on  the  weathered  surfaces.    Thickness,  6  feet. 

13.  Orange  yellow,  calcareous  sand  rock,  containing  crystals  of  calcite.    Thickness, 
13  inches. 

14.  Sandstone,  containing  spherical  concretions.    Thickness,  4  feet. 

15.  Orange  yellow,  calcareous  rock,  as  above.    Thickness,  1  foot. 

16.  Dirty  greenish  white  sandstone,  full  of  the  spherical  concretions  and  blotched 
with  iron  stains.    Thickness,  3  feet. 

17.  Orange  yellow,  calcareous  rock,  with  calcite  crystals  imbedded.    Thickness  15 
inches. 

18.  White  friable  sandstone,  the  upper  foot  filled  with  concretions,  the  lower  three 
and  one-half  with  Scolithus.    Thickness,  4  feet  and  6  inches. 

19.  A  layer  consisting  of  quartzose  sand  cemented  by  calcareous  material,  containing 
calcite  crystals,  and  marked  with  linionite.    Thickness,  8  inches. 

20.  Sandstone  filled  with  concretions.    Thickness,  8  inches. 


PBOFILE  SECTION  OP  BABTHOLOMBW'S 
BLUFF. 


266  GEOLOGY  OF  EASTERN  WISCONSIN. 

21.  Soft,  friable,  dirty  yellowish  sandstone  of  very  uniform  medium  grain.  Thick- 
ness, 6  feet. 

The  concretions  above  referred  to  are  globular  aggregations  of  quaiiz  sand  cemented 
by  calcareous  material,  in  size  and  form,  resembling  a  boy's  marbles.  They  are  fre- 
quently attached  to  each  other,  producing  odd  and  fantastic  fonns. 

On  Mt.  Maria,  two  and  a  half  miles  southwest,  the  main  exposure  is  the  Lower  Mag- 
nesian  limestone,  but  at  the  base  of  it,  at  some  points,  sandstone  is  exposed  and  con- 
tains Scolithus  tubes  within  two  and  a  half  feet  of  the  limestone  above.  On  the  eastern 
slope  of  the  hill  the  calcareous  shales  of  the  Mendota  horizon  may  be  seen. 

Near  the  center  of  section  24  of  the  same  town  the  gulley  of  the  road  exposes  imper- 
fectly a  considerable  portion  of  the  Mendota  formation,  which  is  here  more  shaly  than 
at  Bartholomew's  Bluff  and  does  not  expose  any  firm  thick  layers  of  limestone,  the  sec- 
tion being  composed  chiefly  of  shales  and  sandstones,  as  follows : 

1.  Coarse  yellow  crystalline  limestone,  graduating  into  sandstone.     1  foot. 

2.  Green  and  orange  sandstone  with  calcareous  matter  in  seams  and  aggregations. 
2  feet. 

3.  Green  calcareous  sandstone.    6  inches. 

4.  Orange  sandstone,  1  foot. 

5.  Slope,  covered,  about  3  feet. 

6.  Whitish  sandstone  containing  Scolithus,  3  feet,  3  inches. 

7.  Orange  calcareous  sandstsone,  8  inches. 

8.  Yellow  sandstone  containing  spherical  concretions,  1  foot. 

9.  Calcareous  sandstone,  1  foot. 

Farther  south  the  section  is  extended  upward  about  36  feet,  by  aneroid  measurement, 
and  consists  of  arenaceous  and  calcareous  shales,  interstratified  with  and  graduating  into 
green  sandstone,  and,  more  rarely,  into  gray  sandstone.  Some  of  the  shales  appear 
highly  argillaceous,  and  some  near  the  middle  pass  into  an  impure  limestone.  An  ad- 
jacent hill  is  capped  with  Lower  Magnesian  limestone,  to  whose  enduring  character  it 
owes  its  existence. 

Less  than  a  mile  west  of  this,  Bow's  Hill,  likewise  indebted  to  a  protecting  cap  of 
Lower  Magnesian  limestone  for  its  origin,  presents  along  its  slopes  partial  exposures  of 
the  formation  under  discussion.  At  this  point,  red  and  purple  shales  are  found,  associ- 
ated with  the  various  varieties  of  rock  described  at  the  previous  localities.  These  red 
and  purple  shales  have  already  been  described  as  a  characteristic  of  the  Mendota  group, 
but  as  shown  by  the  previous  sections,  they  are  not  always  present.  These  shales  are 
well  shown  in  the  town  of  Dayton,  Sec.  27,  N.  W.  qr.  of  S.  W.  qr.,  in  a  little  quarry 
along  the  brook  not  far  from  the  road. 

FIG.  25. 


Profile  section  from  N.  W.  to  S.  E.,  across  Green  Lake,  showing  (1,  2  aud  3)  Pofsdara  group,  (2) 
Mendota  beds,  (3)  Madisou  sandstone,  (4)  Lower  Magnesiau  limestone,  (5)  St.  Peters  sandstone, 
and  (6)  Trenton  limestone. 

They  are  again  seen  on  the  shores  of  Green  Lake,  toward  its  western  extremity.  On 
the  south  side  of  the  lake  they  occur  as  a  low  exposure  at  the  water's  edge,  covered  by 
drift.  On  the  opposite  side,  north  of  Norwegian  Bay,  there  is  a  more  considerable  dis- 
play of  Mendota  strata.  The  cliff  has  a  protecting  cap  of  Lower  Magnesian  limestone. 


POTSDAM  SAXDSTOXE.  267 

from  which  descends  a  steep  slope  covered  with  clebns  that  doubtless  conceals  the  Mad- 
ison sandstone,  below  which  there  comes  in  a  series  of  impure  limestone  layers.  These 
are  thin  bedded,  inclined  to  be  shelly,  of  earthy  fracture,  soft  and  quite  argillaceous,  the 
aluminous  material  forming  shaly  partings.  Below  this  follow  a  group  of  arenaceous 
shales  and  shaly  sandstones,  chiefly  of  greenish  and  purple  casts,  whose  structure  is 
somewhat  changeable  as  traced  horizontally.  Oblique  lamination  is  most  beautifully 
shown  in  some  portions.  Underlying  these  are  heavy  beds  of  calcareous  sandstone,  of 
yellowish  color,  and  rather  uniform,  firm  texture,  below  which  lie  purple,  iron-stained 
arenaceous  shales,  succeeded  by  calcareous  sandstone  similar  to  that  above.  The  expos- 
ure reveals  a  low  axis,  the  strata  dipping  both  east  and  west  from  its  center. 

Sugar  Loaf,  on  the  opposite  side  of  the 'Bay,  discovers  essentially  similar  strata.  Sur- 
mounted by  like  Lower  Magnesian  ledges,  its  talus-covered  slope  of  60  feet  is  succeeded 
by  alternating  layers  of  the  Mendota  group. 

Limited  outcrops  of  the  Potsdam  strata  occur  at  several  points  in  Green  Lake  county, 
which  cannot  here  be  specially  described  for  want  of  space,  but  which  the  accompany- 
ing maps  will  enable  any  one  to  identify,  who  may  desire  to  do  so. 

At  Berlin,  adjacent  to  the  porphyritic  ledges,  a  coarse  silicious  sandstone  occurs,  con- 
taining, imbedded  in  it,  fragments  of  the  porphyrite,  often  of  large  size.  These  frag- 
ments are  sometimes  well  worn  and  rounded,  but  oftener  angular.  Fortunately  these 
beds  are  also  fossiliferous,  and  the  following  species  have  been  identified  from  the  col- 
lection made  by  Mr.  F.  H.  King:  Paleophycus,  Sp.  und.,  Orthis  Pepina,  Scolithus,  Con- 
ocephalites  diadematus,  C-,  minor,  C.,  Gibbsi,n.  sp.,  Dicellocephalus  Misa.  These  show 
that  this  sandstone,  conglomerate  and  breccia,  is  of  the  Potsdam  age.  The  position  at 
which  these  occur  in  the  western  part  of  the  state  would  indicate  that  these  beds  belong 
to  the  middle  portion  of  the  formation,  though  the  elevation  as  compared  with  that  of 
the  Lower  Magnesian  limestone,  which  occurs  a  little  to  the  east,  is  such  as  to  lead  to 
the  belief  that  it  belongs  to  a  higher  horizon. 

The  conglomerate  and  breccia  were  undoubtedly  formed  by  the  beating  of  the  waves 
against  the  adjoining  porphyrite  cliffs,  which  formed  a  rocky  island  in  the  ancient  ocean. 

From  this  point  northward  the  Potsdam  beds  are  almost  wholly  concealed  by  drift, 
except  as  a  few  feet  are  exposed  here  and  there  at  the  base  of  the  Lower  Magnesian 
ledges,  that  mark  the  western  Limit  of  that  formation.  Such  exposures  occur  in  the 
towns  of  Winchester,  Caledonia,  Mukwa,  Hortonia,  Ellington,  Cicero,  Shawano  and 
Gillette,  but  nowhere  is  more  than  a  few  feet  of  the  upper  part  of  the  formation  shown. 

Near  the  "  Big  Bend  "  of  the  Oconto  river,  the  bluffs  on  the  south  side  are  crowned 
with  impure  limestone  very  meagerly  exposed,  below  which  the  Potsdam  sandstone  oc- 
casionally shows  itself.  About  two  miles  below  the  bridge,  the  "  Flat  Bock  "  is  formed 
by  beds  of  quartzose  sandstone,  stretching  across  the  river  and  forming  gentle  rapids. 
The  rock  is  grayish  white,  mottled  with  yellow,  and  composed  of  well  rounded  grains  of 
transparent  quartz  of  varying  size,  cemented  with  a  little  calcareous  matter.  The  beds 
dip  gently  to  the  southeast.  The  face  of  the  layers,  as  they  cross  the  river,  is  pitted  with 
"  pot  holes  "  not  often  exceeding  the  size  of  the  homely  utensil  that  gives  them  a  name, 
in  some  of  which  the  gravel  is  still  eddying  about,  continuing  the  process  of  formation. 

At  Little  Falls  on  the  Peshtigo  river,  a  lower  portion  of  the  formation  is  presented, 
consisting  of  white  friable  sandstone,  composed  of  nearly  uniform,  well  rounded  grains 
of  quartz,  with  very  little  cementing  material.  The  upper  beds  are  thick  and  massive; 
below  these,  the  layers  are  thinner  and  softer,  beneath  which  again  are  thicker  beds. 
The  falls  owe  their  origin  to  this  irregularity. 

Several  miles  down  the  river  in  Sec.  12,  T.  31,  R.  20  E.,  there  is  a  low  exposure  con- 
taining Scolithus  tubes,  and  representing  a  higher  horizon. 

The  formation  barely  demonstrates  its  presence  where  it  crosses  the  Menomonee  river' 
into  Michigan. 


268  GEOLOGY  OF  EASTERN  WISCONSIN. 

LOWER  MAGNESIAN  LIMESTONE. 

Reposing  upon  the  upper  face  of  the  Potsdam  sandstone  lies  a 
group  of  silicious  dolomitic  beds,  to  which  the  term  Lower  Magne- 
sian  limestone  was  applied  by  Dr.  Owen,  to  distinguish  them  from 
the  Galena  and  Xiagara  dolomites,  which  constituted  his  Upper  Mag- 
nesian  limestone.  The  former  name  has  very  properly  been  retained, 
while  the  latter,  for  good  reasons,  has  been  discarded.  The  term  Cal- 
ciferous  sandrock,  applied  to  the  near  equivalent  of  the  Lower  Magne- 
sian  limestone  at  the  east,  is  not  admissible  in  this  state,  from  the 
lithological  nature  of  the  rock. 

General  Character.  It  is,  as  the  name  implies,  a  magnesian  lime- 
stone or  dolomite,  sufficiently  pure  to  burn  to  a  serviceable  quicklime 
in  its  lower,  middle  and  upper  portions,  though  not  in  each  layer  of 
these  subdivisions.  The  chief  impurities  are  quartz,  clay,  iron  and 
greensand. 

The  dolomite  occurs  in  the  earthy,  the  granular  crystalline,  and  the 
cryptocrystalline  forms.  The  second  is  the  more  prevalent  form. 
Even  when  the  rock  has  a  decided  earthy  aspect  and  fracture,  exami- 
nation with  a  lens  often  shows  a  large  element  of  crystalline  grains, 
and  on  the  other  hand,  in  most  of  the  cases  where  the  crystals  seem 
to  have  completely  blended  with  each  other,  concealing  themselves  in 
the  common  mass,  the  crystalline  facets  are  apt,  upon  close  examina- 
tion, to  be  more  or  less  discernible,  so  that,  except  where  the  rock  is 
silicious,  the  cryptocrystalline  form  is  not  common.  In  some  por- 
tions the  mass  of  the  rock  is  formed  almost  exclusively  of  small  crys- 
tals of  dolomite,  rather  loosely  aggregated,  leaving  minute,  angular 
spaces  between  the  crystalline  grains,  forming  a  very  pronounced 
granular  rock.  There  are  occasional  evidences  of  what  is  probably 
the  common  fact,  that  this  crystalline  structure  was  assumed  after 
the  deposition  of  the  beds,  and  it  may  have  been  synchronous  with 
their  dolomization.  The  silicious  material  is  present  in  four  princi- 
pal forms:  that  of  dissemination  through  the  mass  of  the  limestone, 
of  concentration  in  nodules  of  chert  or  flint,  of  aggregations  of  quartz 
crystals,  and  of  scattered  grains  of  quartzose  sand. 

The  amount  of  silica  disseminated  through  the  rock  is  less  than,  I 
think,  is  commonly  supposed,  which  is  likewise  true  of  the  quartzose 
sand.  The  granular  character  of  the  rock  causes  it  to  weather  to  a 
harsh  sand-like  surface,  which  appears  more  silicious  than  it  really  is. 
Judging  from  the  analyses  made,  the  silicious  ingredient  rarely  ex- 
ceeds ten  per  cent.,  and  occasionally  falls  below  two. 

The  chert,  of  which  the  quantity,  on  the  whole,  is  large,  is  not  con 


LOWER  MAGNESIAN  LIMESTONE.  269 

fined  to  any  one  horizon,  though  most  abundant  in  the  middle  por- 
tion. Its  distribution  is  irregular,  though  the  nodules  are  frequently 
arranged  in  layers  along  the  bedding  planes  of  the  limestone. 

The  more  distinctly  crystalline  quartz  forms,  in  some  portions  of 
the  deposit,  multitudes  of  little  clusters,  completely  filling  small  cav- 
ities in  the  rock  mass,  and  in  other  portions,  where  the  cavities  are 
larger,  the  crystals  only  form  a  lining,  producing  drusy  little  grottoes, 
some  of  which  are  very  beautiful.  The  quartz  is  most  frequently 
transparent  or  opalescent,  but  it  is  sometimes  red,  brown,  or  rose 
colored.  The  crystals  are  sometimes  grounded  on  a  chalcedonic  base, 
forming  a  beautiful  combination. 

The  quartzose  sand  is  confined  chiefly  to  the  vicinity  of  the  junc- 
tion with  the  sandstone  below  and  above,  and  to  a  subcentral  band  of 
shale,  subsequently  described.  A  portion  of  the  oolitic  grains  Lave  a 
silicious  core. 

Argillaceous  material  is  not  abundant  in  the  formation,  except  in 
shaly  bands,  where  it  sometimes  constitutes  as  much  as  20  per  cent, 
of  the  whole.  In  the  upper  part  of  the  formation  it  sometimes 
amounts  to  six  per  cent.,  but  it  is  seldom  that  the  rock  is  notably  ar- 
gillaceous. Neither  is  the  amount  of  iron  conspicuous,  though  its 
compounds  sometimes  reach  four  or  five  per  cent.  The  rock  seldom 
appears  ferruginous. 

In  addition  to  these  chemical  and  crystalline  characters,  the  oolitic 
structure  distinguishes  some  portions.  In  most  cases,  the  spherules 
differ  but  little  in  size  from  those  of  the  roe  of  our  common  fish, 
which  they  so  much  resemble,  but  some,  as  those  at  Oconto  Falls, 
reach  a  much  larger  size.  It  is  a  significant  fact  that  the  oolitic  struc- 
ture is  confined  to  essentially  the  same  horizon  with  the  sand  above 
mentioned.  A  portion  of  the  spherules  are  simply  grains  of  sand, 
coated  with  concentric  layers  of  carbonate  of  lime  and  magnesia. 

Passing  from  these  to  the  more  massive  features,  the  rock  presents 
a  very  irregular  structure,  owing  to  unevenness  of  hardness  and  com- 
position, and  inequality  of  deposition.  The  effect  of  weathering  is  to 
exaggerate  this,  and  hence  outliers  of  this  formation  present  a  very 
rough  and  often  grotesque  exterior.  A  portion  of  the  rock  is  brecci- 
ated,  having  been  apparently  once  broken  up  by  the  waves,  and  in 
some  cases  somewhat  rounded  by  rolling,  and  afterwards  recemented 
by  material  similar  to  the  fragments  themselves.  These  layers  add 
to  the  coarse  aspect  of  the  rock.  In  addition  to  this,  the  bedding  is 
often  very  irregular,  and  sometimes  obscure,  and  the  beds  not  unfre- 
quently  undergo  change  when  traced  horizontally.  The  color  of  the 
weathered  and  leached  portions  is  a  dirty  white,  gray,  or  very  light 


270  GEOLOGY  OF  EASTERN  WISCONSIN. 

buff  On  the  interior,  the  rock  often  has  a  greenish  blue  or  gray 
cast.  Some  of  the  thinner  beds  and  shaly  layers  are  variegated  with 
red  and  purple.  From  the  ease  with  which  the  sandstone  below  is 
eroded,  the  lower  portion  of  the  formation  is  often  left  projecting  in 
inural  cliffs,  or  forming  a  protecting  crown  for  some  isolated  hill, 
which  owes  its  existence  to  such  defensive  covering.  The  strata  dip 
to  the  eastward,  and  are  soon  lost  beneath  the  later  formations,  by 
penetrating  which  the  formation  may  be  reached  at  continually  in- 
creasing depths,  as  we  go  eastward. 

The  floor  of  the  formation,  so  far  as  has  been  ascertained,  is  essen- 
tially plane,  but  the  upper  surface  is  highly  undulating  or  billowy, 
for  the  latter  term  very  accurately  pictures  to  the  mind  its  remarka- 
ble nature.  The  billows  of  this  petrous  sea  vary  in  height,  from  a 
gentle  swell  to  elliptical  domes  rising  one  hundred  feet  above  their 
bases,  while  their  length  ranges  from  a  few  rods  to  a  quarter  of  a  mile 
or  more,  and  their  width,  from  one-third  to  one-half  the  length.  The 
regularity  of  outline  here  indicated  is  a  frequent  and  typical,  but  not  uni- 
versal, fact.  The  slope  of  the  sides  varies  from  30°  downwards.  The 
axes  of  these  domes  lie  in  an  easterly  and  westerly  direction,  much 
more  commonly  than  otherwise. 

FIG.  26. 


EAST  AND  WEST  SECTION  NEAR  RIPON*. 
1.  Lower  Magnesian  limestone.    2.  St.  Peters  sandstone.    3.  Trenton  limestone. 

The  superficial  strata  of  these  rock-billows  dip  in  every  direction 
from  the  center,  most  rapidly  at  the  sides,  and  less  so  at  the  extremi- 
ties; or,  in  other  words,  they  are  essentially  concentric  with  the  sur- 
face. 

These  statements  are  made  with  reference  to  the  original  condition 
of  the  mounds  before  erosion.  There  are  satisfactory  evidences  that 
during  the  deposit  of  the  St.  Peters  sandstone  upon  this  unequal  sur- 
face, the  exterior  of  these  prominences  was  somewhat  eroded,  and  in 
the  removal  of  the  latter  formation  by  the  elements  and  the  drift 
forces,  resulting  in  their  present  exposure,  they  were  still  further  acted 
upon. 

The  eastern  and  northeastern  extremities  suffered  considerable  abra- 
sion from  the  latter  cause.  But  neither  of  these  agencies  modified, 
except  superficially,  the  form  of  these  prominences,  while  they  served 
to  demonstrate  more  satisfactorily  the  quaquaversal  character  of  the 
dip. 


LOWER  MAGNESIAN  LIMESTONE.  271 

Unfortunately,  little  is  positively  known  to  me  concerning  their  in- 
terior. The  deeper  strata  observed  were  of  very  irregular  character, 
being  either  brecciated  or  showing  a  tendency  to  a  rude  concretionary 
grouping  of  material  into  irregular  lump-like  enlargements  of  the  lay- 
ers. In  a  very  few  instances,  supposed  to  belong  to  this  class,  nota- 
bly an  outlier  one  mile  south  of  the  village  of  Markesan,  the  whole 
of  the  rock  exposed  is  a  thoroughly  brecciated  mass,  with  obscure  or 
absent  bedding  lines.  This  may,  perhaps,  be  the  remnant  of  a  larger 
mass  that  formed  the  nucleus  over  which  the  sloping  strata  were  de- 
posited, for  the  weight  of  evidence  goes  to  show  that  this  is  a  phenom- 
enon of  deposition  and  not  of  upheaval. 

FIG.  27. 


SECTION  (north  of  Stiles)  SHOWING  THE  RELATIONS  OF  THE  ST.  PETERS  SANDSTONE  AND  LOWER 
MAONESIAN  LIMESTONE. 

Organic  Remains.  These  are  very  meager.  Fucoidal  remains, 
Salterella(?),  an  undetermined  species  of  Stromatopora, ;  Ophileta  uni- 
angulata,  two  undetermined  species  of  Trilobites,  doubtfully  referred 
to  the  genus  Barthyurus,  embrace  those  found  in  this  region. 

Area.  It  has  been  remarked  that  the  Potsdam  sandstone  area 
forms  a  rude  crescent,  the  eastern  limb  of  which  enters  the  district 
under  consideration  in  Green  Lake  county,  and  extends  thence  to  the 
Menomonee  river.  The  Lower  Magnesian  limestone  forms  a  serrated 
band  or  a  fringe  on  the  convex  edge  of  this  crescent,  averaging  about 
seven  miles  in  breadth.  It  barely  enters  the  district  on  the  western 
margin  of  the  counties  of  Jefferson  and  Dodge,  but  invades  Green 
Lake  county  with  its  full  width,  and  thence  passes  diagonally  on- 
ward to  the  northeast,  through  Winnebago,  Outagamie,  Shawano, 
and  Oconto  counties,  as  exhibited  on  the  accompanying  maps. 

Thickness.  Owing  to  the  uneven  surface,  the  thickness  varies 
greatly.  The  observed  extremes  in  this  region  are  62  feet  and  141 
feet.  Calculations  based  on  dip  give  very  similar  results,  but  it  is 
highly  probable  that  the  thickness  sometimes  exceeds  these  limits. 

Local  Descriptions.  The  most  southerly  point  at  which  the  Lower  Magnesian  lime- 
stone appears  within  the  eastern  district,  is  at  Waterloo,  in  Jefferson  county.  Along 
the  stream  below  the  lower  bridge,  at  the  village,  a  low  ledge  presents  its  rough,  weath- 
ered face  to  view.  It  consists  of  a  coarse,  cherty,  buff,  silicious  dolomite,  in  medium 
beds  of  rough,  uneven  texture,  owing  in  part  to  irregular  cavities  and  granular  porous 


272  GEOLOGY  OF  EASTERN  WISCONSIN. 

spots,  and  in  part  to  the  presence  of  nodules  of  chert.  This  inequality  of  structure  is 
exaggerated  by  the  effects  of  long  weathering,  giving  the  surface  a  very  ragged  aspect. 
The  exterior  of  the  chert  is  usually  white  and  rather  soft,  while  the  interior  is  dark  or 
reddish,  hard,  translucent  and  flint-like.  The  outcrop  represents  the  upper  portion  of 
the  formation. 

Tin's  limestone  next  appears  to  the  north,  within  our  district,  on  the  Crawfish  river,  two 
miles  below  Columbus,  in  a  low  exposure  in  the  banks  of  the  stream,  similar  to  the 
above.  Three-quarters  of  a  mile  northeast  from  this,  near  the  center  of  the  S.  E.  ^ 
sec.  19,  town  of  Elba,  a  quarry  exposes  the  following  section  of  impure  magnesian  lime- 
stone: 

1.  A  brecciated  stratum,  composed  of  small,  compact,  dark  gray  fragments  between 
which  are  numerous  irregular  spaces  filled  with  white  pulverulent  material.    Thickness, 
2  feet. 

2.  Beds  more  homogeneous  than  the  above,  yet  porous  in  parts  and  compact  in  oth- 
ers, containing  nodules  of  chert.    Thickness,  4-6  feet. 

3.  A  very  highly  brecciated  layer,  formed  of  compact,  dark  colored  dolomitic  frag- 
ments, covered  with  black  dendritic  crystals,  and  full  of  small,  irregular  crystal  lined  cav- 
ities.   Thickness,  1.45  feet. 

4.  A  stratum  of  very  uneven  texture  and  composition,  containing  silicious  nodules. 
Thickness,  5. 7  feet. 

5.  A  single  thick-bedded,  porous,  moderately  soft  dolomitic  layer  of  uneven  texture. 
Thickness,  2.3  feet. 

6.  A  band  of  rather  thin  sheets  of  irregular  arrangement,  inclosing  large,  coarse,  nod- 
ular masses  of  breccia-like  rock,  hard,  compact,  cherty,  red  stained,  some  portions  ap- 
parently silicious,  some  nearly  pure  dolomite.    Thickness,  4.35  feet. 

7.  Thick,  uniform  bed    of  moderately  hard,  compact  texture,  the  upper  portion 
marked  with  greenish  silicious  sand,  iron  stained.  Thickness,  2. 75  feet.  Total,  21 . 15  feet. 

North  of  this,  in  Dodge  county,  this  formation  shows  an  occasional  limited  exposure, 
similar  to  the  preceding. 

In  Green  Lake  County  it  has  already' been  remarked  that  the  Lower  Magnesian 
strata  crown  several  of  the  prominent  hills.  These  are  the  lower  layers  of  the  forma- 
tion, and  constitute  the  small  patches  lying  west  of  the  serrated  edge  of  the  main  body 
of  the  formation,  as  represented  on  the  accompanying  maps. 

The  extensive  prairies  of  Manchester  and  Dayton  townships  are  underlaid  by  this 
rock,  while  those  to  the  eastward  repose  on  the  Trenton  and  Galena  limestones.  It  is 
in  this  county  that  we  first  find  a  clear  demonstration  of  what  constitutes  the  most  re- 
markable feature  of  the  Lower  Magnesian  limestone,  viz. :  the  undulatory  nature  of  the 
upper  face  of  the  formation  already  mentioned.  North  of  Lake  Maria,  in  the  town  of 
Mackford,  are  several  conical  mounds,  partially  covered  with  earth,  which  rise  nearly 
to  the  level  of  the  base  of  the  Trenton  limestone,  which  occurs  a  few  rods  to  the  east, 
while  in  the  town  south,  at  least  23  feet  of  sandstone  intervene,  and  in  the  town  north, 
at  least  82  feet,  and  near  Eipon,  over  100  feet.  So  far  as  exposed,  the  strata  forming  the 
mounds  dip  away  from  the  center.  But  we  need  not  linger  upon  so  poor  an  exposure. 

In  the  S.  E.  qr.  of  Sec.  7  of  the  same  town  is  a  conical  hill  surmounted  by  a  turret 
of  massive  breccia,  which  needs  to  be  noted  in  this  connection,  though  there  is  nothing 
except  its  elevated  position  to  show  that  it  indicates  any  irregularity  in  the  surface  of 
the  formation.  But  in  the  N.  E.  qr.  of  Sec.  15  of  the  same  town,  at  the  point  where 
the  road  crosses  a  small  stream,  there  is  a  most  satisfactory  demonstration  of  this  in  the 
rise  of  an  arch  of  Lower  Magnesian  strata  into  actual  contact  tvith  the  Trenton  lime- 
stone, causing  the  thinning  out  of  the  St.  Peters  sandstone  to  absolute  zero.  This  is  il- 
lustrated by  the  accompanying  figure. 

The  layers  of  the  Lower  Magnesian  at  tin's  point,  especially  as  seen  down  the  stream 


LOWER  MAGNESIAN  LIMESTONE.  273 

a  few  rods,  consist  of  two  classes,  thin  undulating  beds  and  thick  brecciatsd  ones;  the 
two  alternating,  in  a  measure,  with  each  other.  The  latter  are  very  hard  and  crystalline 
in  texture.  Some  of  the  angular  cavities  that  constitute  the  interspaces  between  the 
fragments  of  the  breccia  are  filled  with  calcite  and  pyrites,  but  most  of  them  are  empty, 
giving  the  impression  that  the  rock  had  been  crushed.  But  this,  with  one  or  two  other 
similar  cases,  is  exceptional.  The  breccias  that  are  so  common  a  feature  in  this  lime- 

FIG.  28. 


1.  Lower  Magnesian  Limestone.    2.  St.  Peters  Sandstone.    3.  Trenton  Limestone. 

stone  cannot,  in  my  judgment,  be  satisfactorily  explained  by  any  form  of  crushing  after 
deposition.  In  this  instance  the  undulatory  nature  of  the  thin  beds,  and  the  hardness 
and  crystalline  character  of  the  brecciated  rock  lend  some  plausibility  to  the  idea  of  com- 
pression, or  forcible  upheaval,  as  the  cause  of  this  apparent  flexure  of  the  Lower  Magne- 
sian strata.  But  we  shall  have  occasion  to  consider  a  large  mass  of  facts  not  in  conso- 
nance with  such  a  view. 

The  figure,  which  exhibits  an  east  and  west  section,  shows  that  the  strata  dip  in  both 
those  directions,  and  by  following  down  the  stream  to  the  northward,  they  are  seen  to 
slope  rapidly  in  that  direction  also.  To  the  south  they  are  concealed,  but  judging  from 
analogy,  they  descend  also  in  that  direction  within  a  short  distance,  thus  forming  n 
dome  supporting  the  Trenton  strata  above. 

The  character  of  the  sandstone,  which  will  be  considered  more  fully  under  its  appro- 
priate head,  makes  it  evident  that  the  sides  of  this  dome  were  subject  to  the  action  of 
the  waves  while  the  St.  Peters  sandstone  was  being  deposited,  demonstrating  that 
whatever  cause  produced  the  arch,  acted  before  the  sandstone  was  formed. 

In  sections  one  of  this  town  and  thirty-six  of  the  town  north,  the  Lower  Magnesian 
and  Trenton  strata  are  found  at  the  same  level  and  very  near  each  other,  leaving  no 
doubt  that  here  is  another  instance  of  the  lower  formation  rising  into  the  horizon  of-  the 
upper.  This  is  shown  by  Fig.  19,  ante  p.  251. 

Six  miles  to  the  west  of  this,  on  the  shores  of  the  Little  Green  Lake,  the  same 
peculiarity  is  again  manifested.  At  the  southeast  angle  of  the  lake,  a  low  arch  is  par- 
tially exposed,  while  on  the  north  shore  a  more  decisive  instance  occurs.  A  precipitous 
bluff,  crowned  with  Trenton  strata,  skirts  the  lake  on  that  side.  At  the  west  end  of  this 
bluff,  there  are  fifty-four  feet  of  St.  Peters  sandstone  between  the  Trenton  layers  and  the 
water's  edge,  and  how  much  is  concealed  beneath  is  unknown.  But  within  eighty  rods 
to  the  east,  the  Lower  Magnesian  strata  rise  above  the  water's  edge,  and  approach 
within  eighteen  feet  of  the  Trenton  above,  if,  indeed,  they  do  not  come  into  actual  con- 
tact, as  the  nature  of  the  slope  seemed  to  indicate,  but  which  could  not  be  observed  on 
account  of  the  talus  covering  the  side  of  the  bluff.  In  the  opposite  direction,  within  a 
half  mile,  the  Lower  Magnesian  strata  may  be  found  arching  upwards  to  elevations  of 
thirty  and  forty  feet,  or  more,  above  the  lake  level. 

About  half  a  mile  to  the  northwest,  a  valley  reveals  the  arcuate  nature  of  the  strata 

most  clearly.     On  entering  the  gorge  below,  the  layers  are  found  to  dip  southward  at 

an  angle  of  20°  and  upwards,  but  as  the  crest  is  mounted,  the  inclination  becomes  lesd 

and  less  until  they  are  lost  beneath  the  soil,  within  twenty  feet  of  the  Trenton  horizon. 

Wis.  SUR.  — 18 


274:  GEOLOGY  OF  EASTERN  WISCONSIN. 

Toward  the  top,  there  are  to  be  found  some  very  sandy  layers  that  appear  to  rest,  in  a 
measure,  unconformably  upon  a  worn  surface  beneath,  and  probably  represent  the  St. 
Peters  sandstone,  which  would  naturally  be  calcareous  in  such  a  situation. 

A  portion  of  the  rock  of  this  dome  is  a  coarsely  brecciated,  very  hard  crystalline  dolo- 
mite, but  the  greater  part  belongs  to  the  more  common  class  of  coarse,  impure  magne- 
sian  limestone  that  characterizes  this  formation. 

Passing  by  a  number  of  minor  exhibitions  of  the  same  phenomena,  we  find,  in  the 
vicinity  of  Ripon,  this  peculiarity  developed  to  a  wonderful  extent.  Just  west  of  the 
Ceresco  Mills,  in  the  lower  part  of  the  city,  there  rises  a  rock  hill,  having  an  elongated 
oval  contour,  somewhat  enlarged  and  curved  at  the  eastern  extremity.  Its  base  is 
skirted  on  the  east  and  north  by  streams  above  which  its  crest  rises  to  an  average  height 
of  about  one  hundred  feet.  Its  axis  lies  east  and  west,  and  does  not  much  exceed  one- 
fourth  of  a  mile  in  length.  It  is  terminated  at  the  west  by  a  deep  ravine,  beyond  which 
rises  a  second  ridge  of  similar  form  and  height,  and  somewhat  greater  length,  but  which 
is  less  conspicuous  because  of  its  connection  with  the  plateau  on  the  south.  The  ridge 
first  mentioned  is  nearly  isolated  by  a  deep  ravine  on  the  south,  which  reveals  its  form, 
though  the  rock  exposures  are  chiefly  confined  to  the  eastern  end.  On  the  northeast 
slope,  thick,  heavy,  rough  beds  of  Lower  Magnesian  limestone  show  a  dip  of  15°  to  18° 
to  north  of  east.  On  the  easternmost  point,  the  dip  is  18°  to  the  eastward,  while  on  the 
southeast  curve  a  slant  of  25°  to  30°  to  the  southeast  is  observed,  and  farther  along  the 
south  side  of  the  hill,  a  more  southward  and  southwestward  dip  seems  to  be  indicated, 
though  the  exposures  are  very  unsatisfactory.  A  small  quarry  above  the  limekiln,  and 
near  the  top  of  the  hill,  shows  within  itself  dips  of  3°  E.,  12%°  N.  E.,  and  7°  N.  W., 
with  ah1  intermediate  inclinations.  This  irregularity  is  not  caused  by  the  folding  or  con- 
tortion of  even  bedded  layers,  so  much  as  by  the  thickening  and  thinning  of  irregular 
'ones.  Great  lumps,  as  it  were,  occur  at  certain  points,  swelling  two  or  three  fold  the 
thickness  of  the  layer,  or  causing  it  to  disappear  entirely  in  a  structureless  mass.  The 
rock  is  greenish  blue,  somewhat  argillaceous,  aud  contains  a  few  fossils. 

Down  the  slope  from  this  quarry,  and  within  six  rods  of  it,  a  bed  of  St.  Peters  sand- 
stone lies  immediately  against  the  flank  of  the  Lower  Magnesian  arch,  the  top  of  the 
sandstone  being  30  feet  below  the  crest  of  the  ridge.  The  actual  junction  of  the  sand- 
stone with  the  limestone  was  not  visible  at  the  time  of  either  of  my  visits,  but  I  was 
credibly  informed  that  in  a  filled  portion  of  the  sand  pit  it  had  been  previously  exposed. 

Wells  in  the  vicinity  show  that  the  surface  of  the  limestone  descends  to  at  least  100 
feet  below  the  top  of  the  hill.  There  is  here  then  within  a  horizontal  distance  of  less 
than  one  quarter  of  a  mile,  a  rise  and  fall  of  the  upper  limits  of  the  Lower  Magnesian 
limestone  of  not  less  than  100  feet. 

FIG.  29. 

382ft. 


AND  SOUTH  SECTION,  NEAB  RIPON. 
1.  Lower  Magnesian  limestone.    2.  St.  Peters  sandstone.    3.  Trenton  limestone. 

Within  less  than  a  half  mile  south  of  this  arch,  the  Lower  Magnesian  strata  again 
mount  into  the  Trenton  horizon,  more  than  100  feet  above  the  intervening  depression, 
and  again  to  the  south,  less  than  half  a  mile,  another  arch  appears,  but  passes 
under  the  bluff  to  the  west  before  attaining  so  great  an  altitude  as  the  two  preceding 
ones.  The  rock  forming  this  one  is  unusually  irregular  in  hardness,  and  weathers  out 
into  the  most  fantastic  shapes,  so  that  the  loose  worn  masses  are  much  admired  as  lawn 
ornaments. 

The  accompanying  figure  will  assist  in  illustrating  the  foregoing  facts.    The  irregu- 


LOWER  MAGNESIAN  LIMESTONE. 


275 


larity  is  unquestionably  due  chiefly  to  the  undulation  of  the  uppei'  strata  of  the  forma- 
tion; but  there  is  evidence  that  the  sides  of  these  prominences  were  somewhat  worn  by 
wave  action  daring  the  deposit  of  the  St.  Peters  sandstone  and  a  portion  of  the  rock 
incorporated  in  that  formation.  Near  the  west  line  of  the  township  of  Ripon,  on  the 
lowlands,  near  the  ledge  that  marks  the  limit  of  the  Trenton  plateau,  the  upper  por- 
tion of  one  of  these  swells  is  finely  shown.  It  is  only  a  few  rods  in  extent,  and  attains 
but  a  meager  elevation  compared  with  those  just  described.  It  is  oval  and  symmetrical 
in  outline,  and  has  its  greater  axis,  which  is  about  twice  its  transverse  diameter,  east 
and  west,  in  harmony  with  the  general  rule.  The  surface  rock,  which  alone  is  exposed, 
is  rather  even  bedded  and  homogeneous  for  this  formation,  in  which  irregular  structure 
is  the  prevalent  form. 

West  of  Rush  Lake,  at  several  points,  the  billowy  character  of  this  face  of  the  for- 
mation is  shown  by  variously  dipping  strata  and  half  exposed  domes  of  rock. 

In  the  railroad  cut  adjacent  to  the  lake  shore,  near  the  center  of  section  15,  Nepeuskin, 
something  of  the  nature  of  the  interior  of  these  mounds  is  revealed,  though  the  cut  does 
not  exceed  six  feet  in  depth.  The  surface  of  the  rock  is  irregularly  undulating,  consist- 
ing of  hummocks  and  hollows;  notwithstanding  which,  it  is  interesting  to  note  that  it 
is  polished  and  covered  with  glacial  strise,  bearing  westward.  It  might  be  supposed 
that  the  present  surface  is  due  to  erosion,  were  it  not  for  a  sandy  layer,  coveiing  a  por- 
tion of  the  surface,  that  seems  to  belong  to  the  sandstone  subsequently  deposited.  The 
rock  is  very  irregular  in  bedding  and  stratification.  The  layers  thicken  and  thin,  enter 
and  disappear,  in  a  very  remarkable  way,  and  that  within  the  space  of  a  few  feet.  At 
the  same  time  they  curve  and  dip  in  various  degrees  and  directions.  The  accompany- 
ing cuts,  from  sketches  made  on  the  spot,  will  serve  to  show  this  imperfectly. 

FIG.  30. 


SKETCHES  FROM  SECTION  15,  NEPEUSKIN. 
Showing  irregular  structure  of  Lower  Magnesian  limestone. 

The  irregularity  is  such  that  it  seems  necessary  to  attribute  it  to  the  conditions  of  de- 
position and  not  to  subsequent  disturbance.  During  the  process  of  deposition  there  ap- 
pears to  have  been  more  or  less  of  loosening,  breaking  up,  rounding  and  rearranging  of 
the  somewhat  indurated  sediment  and  its  redeposit,  intermixed  with  finer  material,  but 
after  the  final  deposition  there  is  no  evidence  of  subsequent  disturbance  beyond  that 
common  to  all  formations.  Northwest  of  Winneconne  these  mounds  become  so  pre- 
valent that  the  surface  of  the  formation  may  very  fittingly  be  termed  billowy.  They 
seldom  exhibit  a  greater  length  than  forty  rods,  nor  an  elevation  of  more  than  thirty  or 
forty  feet,  and  are  usually  much  less  than  this.  Of  course  mention  is  here  made  only  of 
that  portion  which  protrudes  above  the  drift,  and  not  of  the  actual  dimensions.  Their 
greatest  length  here,  as  elsewhere,  is  east  and  west.  The  dip  in  all  cases,  so  far  as 


276  GEOLOGY  OF  EASTERN  WISCONSIN. 

could  be  determined,  was  quaquaversal,  being  greatest  on  the  sides  and  perceptibly  less 
at  the  extremities.  The  greatest  dip  observed  in  this  vicinity  was  20°.  In  most  cases 
apparently  only  the  crest  of  the  arch  was  exposed  and  the  dips  were  low. 

One  of  these  hills,  situated  near  the  center  of  the  east  line  of  section  15  of  the  town  of 
Winneconne,  presents  some  special  features  deserving  mention.  The  uppermost  layer, 
where  still  preserved,  contains  a  large  ingredient  of  quartzose  sand,  or  is  incrusted  with 
sand,  or  in  other  cases,  consists  of  a  conglomerate  or  breccia  whose  matrix  is  quartzose 
sand.  This  layer  is  also  sometimes  oolitic.  As  similar  facts  were  observed  at  several 
other  widely  separated  localities,  this  sandy  portion  is  believed  to  be  the  transition  layer 
to  the  St.  Peters  sandstone,  and  if  so,  it  indicates,  where  preserved,  the  original  form 
of  'these  mounds,  and  that  in  these  instances  the  drift  forces  have  only  removed  the  in- 
coherent sandstone  above.  This  is  rendered  the  more  probable  by  the  fact  that  usually 
this  sandy  layer  was  found  on  the  southivestward  side  of  the  prominence,  where  it  would 
be  protected  from  the  more  forcible  action  of  the  glacier,  while  the  northeastern  comer, 
which  sustained  the  full  force  of  the  ice  mass  coming  from  that  direction,  was  often  con- 
spicuously abraded. 

Another  interesting  fact  observed  at  this  point  was  the  presence  of  distinct  mud- 
cracks  and  ripple  marks.  The  latter  are  far  less  common  on  limestone  than  on  sand- 
stone, and  the  former  are  more  abundant  in  shales.  Both  occur  here  together  on  the 
gentle  slope  of  one  of  these  peculiar  mounds.  The  dip,  here,  varies  from  0  to  8°,  con- 
forming as  usual  to  the  shape  of  the  hill,  which  in  this  case  departs  somewhat  from  the 
usual  symmetrical  contour.  The  rock  structure  is  very  irregular.  Some  portions  arc  a 
well  marked  conglomerate,  both  matrix  and  pebbles  being,  however,  dolomitic.  A  layer 
near  the  surface  is  very  fossiliferous,  over  the  small  space  exposed,  but  the  casts  are  so 
obscure  as  to  preclude  satisfactory  specific  determinations.  They  consist  of  the  internal 
casts  of  an  Ophileta  and  two  undetermined  species  of  Raphistoma. 

While  our  attention  has  thus  been  fastened  upon  the  peculiarities  of  the  superior  face 
of  the  Lower  Magnesian  formation,  we  have  been  led  northward  along  the  eastern  mar- 
gin of  the  outcrop,  where  alone  the  upper  portion  has  escaped  erosion,  and  have  passed 
by  some  noteworthy  outcrops  belonging  to  the  middle  and  lower  parts  of  the  formation. 
If  we  now  return  to  the  vicinity  of  the  village  of  Eureka  we  shall  be  introduced  to  a 
feature  that  characterizes  the  submedian  portion  of  the  formation.  The  ledge  south- 
west of  that  place  presents  the  following  section  in  descending  order: 

1.  Heavy  irregular  beds  of  impure  dolomite,  containing  many  cavities,  more  or  less 
filled  with  quartz  crystals  of  the  transparent  and  milky  varieties;  texture  varying;  bed- 
ding uneven  and  somewhat  undulatory;  rock  weathers  to  a  very  rude  ragged  aspect. 
Thickness,  10  feet. 

2.  Reddish  shale,  variegated  with  gray  and  green,  the  lower  portion  mostly  soft,  break- 
ing and  crumbling  easily;  some  parts  quite  arenaceous;  the  upper  portion  more  calcare- 
ous or  dolomitic,  and  containing  many  aggregations  of  quartz  crystals,  usually  of  the 
opalescent  variety.    The  layers  are  irregular  and  somewhat  undulating.     Thickness,  15 
feet. 

3.  Very  heavy  beds,  nearly  uniform  in  thickness,  and  horizontal  in  bedding.    The 
rock  contains  many  almond-sized  but  irregular  cavities,  only  a  small  proportion  of  which 
are  filled  with  crystals.     It  is  uneven  but  distinctly  granular  crystalline  in  texture,  me- 
dium in  hardness,  and  dirty  gray  or  buft'  on  the  exterior,  but  mottled  bluish  on  the  in- 
terior.    It  is  well  adapted  to  heavy  masonry,  as  foundations,  piers  and  locks.     It 
is  used  for  the  latter  purpose  in  the  construction  of  the  adjacent  locks  on  the  Fox  river. 
Thickness  exposed,  6  feet. 

Attention  is  here  called  to  the  shale  which  constitutes  the  middle  member  of  the  sec- 
tion. What  appears  to  be  the  stratigraphical  equivalent  of  this,  occurs  at  several  points 
to  the  northward,  the  most  remote  being  over  one  hundred  miles  distant.  From  this 


LOWER  MAGNESIAN  LIMESTONE.  277 

fact  it  has  a  value  as  a  guide  in  fixing  the  position  of  the  subordinate  divisions  of  the 
formation. 

In  speaking  of  the  sandstone  below,  mention  has  already  been  made  of  several  locali- 
ties in  Green  Lake  county,  where  the  lower  strata  of  this  formation  are  visible  chiefly  in 
the  position  of  protecting  caps  covering  sandstone  hills. 

Mt.  Tom,  in  the  township  St.  Marie,  while  affording  another  example  of  this,  exposes 
a  considerable  group  of  the  bottom  layers  of  the  Lower  Magnesian  limestone  as  follows, 
in  descending  order: 

1.  Rough,  silicious,  congloineritic  dolomite,  of  dirty  gray  aspect,  weathering  to  a  very 
ragged  surface,  which  develops  prominently  its  conglomeritic  character,  and  also  the 
many  aggregations  of  white  quartz  crystals  that  abound  in  it;  rather  thick  bedded. 
Entire  thickness  of  original  stratum  not  known,  as  it  fonns  the  apex  of  the  hill.   28  feet. 

2.  Light  bluish  gray,  thin  bedded  dolomite  of  even,  fine  grained  texture,  and  easy, 
regular,  earthy  fracture,  which  would  render  it  very  excellent  for  building  purposes  if 
the  courses  were  thicker,  as  they  probably  would  be  found  to  be  where  less  affected  by 
surface  agencies.    4  feet. 

3.  A  thick,  rough,  brecciated  bed  similar  to  No.  1  above.     2  feet. 

4.  Shelly,  magnesian  limestone  and  calcareous  shale.    The  layers  are  thickest  and 
most  calcareous  at  the  top,  becoming  thinner  and  graduating  into  the  more  shaly  por- 
tion below,  which  is  grayish  buff  and  purple,  and  appears  to  be  quite  arenaceous,  though 
not  so  in  fact.    8  feet. 

5.  Coarse,  rough,  thick  bedded,  dirty  gray,  hard,  granular,  silicious  dolomite,  contain- 
ing small  inconspicuous  geodes;  irregularly  cracked  and  fissured,  and  frequently  form- 
ing over-hanging  ledges  from  the  removal  of  the  softer  sandstone  below.     15  feet. 

.    On  the  slope  below  the  limestone  occasional  slight  exposures  of  red  and  yellow  Pots- 
dam sandstone  are  visible. 

In  sections  11  and  14  of  Brooklyn,  in  this  county,  the  beds  exposed  are  unusually 
geodiferous.  Nearly  or  quite  half  the  volume  of  the  rock  in  some  cases  is  formed  of 
cavities  lined  with  quartz  crystals.  These  are  chiefly  red,  brown  and  pink,  sometimes 
forming  very  handsome,  though  small  and  irregular  geodes.  At  numerous  other  points 
in  Green  Lake  county,  there  are  slight  outcrops  of  this  formation,  which  do  not  merit 
special  description,  but  which  may  be  readily  identified  by  the  characteristics  already 
given,  or  by  reference  to  the  accompanying  maps. 

In  the  town  of  Poygan,  Winnebago  county,  the  western  limit  of  this  formation  is 
marked  by  a  line  of  bluffs,  along  the  face  of  which  occasional  outbreaks  of  the  strata 
occur,  but  no  conspicuous  escarpments. 

In  the  N.  W.  qr.  of  Sec.  26,  a  quarry  has  been  opened  and  a  kiln  constructed  for  the 
purpose  of  manufacturing  hydraulic  and  quicklime.  At  the  top  of  the  quairy,  three  feet 
of  thin-bedded  undulatory  layers  of  magnesian  limestone  are  burned  for  the  latter  pur- 
pose. Below  this  is  a  layer  exhibiting  very  unequal  deposition,  whose  irregularities  seem 
to  give  rise  to  the  wave-like  nature  of  the  beds  above.  This  is  underlaid  by  sixteen  feet 
of  a  rather  soft,  granular,  argillaceous,  magnesian  limestone  of  a  slightly  olivaceous 
gray  color,  which  disintegrates  readily  when  acted  on  by  the  elements.  The  beds  are 
below  medium  thickness,  and,  in  some  cases,  furnish  good  flagging,  and  the  material 
from  which  the  waterlime  is  prepared,  At  the  base  is  one  foot  of  a  yellowish-gray  rock, 
eight  inches  of  decomposed  rotten  stone,  reposing  on  the  common  hard  dolomite  of  the 
formation,  which  is  very  slightly  uncovered. 

In  the  erosion  of  the  Wolf  river  valley,  in  Caledonia,  Mukwa  and  Hortonia,  the 
sandstone  below  was  readily  removed  and  the  more  resisting  ledges  of  dolomite  left  pro- 
jecting in  vertical  cliffs  of  moderate  height.  By  combining  the  facts  exhibited  at  several 
points  along  this  line  of  ledges,  chiefly  those  in  Hortonia,  the  following  section,  rep- 
resenting about  60  feet  of  the  base  of  the  formation,  was  obtained. 


278 


GEOLOGY  OF  EASTERN  WISCONSIN. 


Earth. 

1.  Carved  strata  of  hard,  compact,  flint-like,  bluish  dolomite.    18  inch  if. 

2.  Compact  bluish  white  dolomite.    Purest  layer.    13  inches. 

3.  White  compact  dolomite,  with  quartz  in  layers,  at  the  bedding  j^-d'd.    28 

inches. 

4.  Compact  whitish  dolomite,  similar  to  the  above,  but  less  silicious.    ?i>  ir  Aties. 
Unexposed.    ti  to  7  feet. 


5.  Blue  compact  hard  dolomite,  somewhat  sijicious.    9  inches. 

6.  Yellow,  fine-grained  dolomite,  softer  than  the  above.    3  feet. 

7.  Thin  sandy,  argillaceous  layer.    1  inch. 

8.  Thin  bedded  dolomite,  suitable  for  lime.    12  inches. 

9.  Fine  grained,  but  rough  bedded  dolomite.    3  feet. 


10.  Thinner  bedded,  compact  dolomite.    3  feet. 


11.  Thin,  shelly,  sandy  layer.    10  inches. 

12.  Unexposed.    3  feet. 


13.  Mottled  brecciated  dolomite.    18  inches. 

14.  Very  rotten,  chippy  layer.    18  inches. 

15.  Brecciated  mo:tled  layer,  as  above.    18  inches. 


^J*^    — -     16.  Thick  bedded,  rough,  uneven-textured  dolomite.    6  feet. 


17.  Shelly  rotten  layer.    3  feet. 


18.  Not  exposed.    3  feet. 


r^^VV?""  19-  RouBn'  uneven-tex*.ured  dolomite.    1  foot. 


20.  Flinty  layer.    4  inches. 

^-—  21.  Somewhat  sandy,  dolomitic  limestone.    4  inches. 
ta->i^  22.  Rough,  irregular  dolomite.    3  feet. 


!23.  Sandy  layer.    1  foot. 

2J.  Light  colored,  slightly  silicious  and  moderately  hard  dolomite.    2  feet. 

25.  Broken  rotten  layer.    14  inches. 
^ZT^Zlf      2ti-  Silicious,  dolomitic  limestone,  very  hard  and  flint-like.    2  feet  and  9  inches. 


27.  White  sandstone,  marked  with  green.    4  inches. 

28.  Sandy  layer.    3  inches. 

-  —       29.  Similar  to  No.  26.    3  feet  and  3  inches. 


30.  Oolitic  layer.    4  inches. 

31.  Coarsely  brecciated  layer,  chiefly  sandstone,  but  with  some  quartz  and  quart- 

zite-like  rounded  and  angular  masses.    4  feet  and  2  inches. 


32.  Coarse  friable  sandstone  of  uniform  grain,  and  containing  nodules  of  iron 
ore.    Quartzite-like  layer  near  the  top.    3  feet  and  3  inches. 

Unexposed. 


LOWER  MAGNESIAN  LIMESTONE. 


279 


In  tracing  the  layers  along  the  face  of  these  natural  walls,  they  show  much  tendency 
to  change,  and  it  is  only  by  close  observation  and  great  care  that  an  accurate  correlation 
of  different  sections  can  be  made,  and  considerable  variation  is  to  be  expected  where 
much  distance  intervenes. 

This  changeableness  will  be  manifest  by  comparing  the  preceding  section  with  the 
two  following,  both  taken  from  the  same  quarter  section  (S.  W.  qr.  Sec.  25,  Mukwa). 


FIG.  32. 


1.  Earth. 

2.  Magnesian  limestone.    30  inches. 

3.  White  sandstone.    3  inches. 

4.  Magnesian  limestone.    8  inches. 

5.  Oolitic  silicious  limestone.    7  inches. 

6.  Magnesian  limestone.    9  inches. 

7.  Sandstone.    8  inches. 

8.  Thick  even-bedded  magnesian  limestone.    34  inches. 


9.  Oolitic  silicious  limestone.     5  inches. 


3xi£777-    10.  Sandy  magneeian  limestone  of  irregular  hcdding  and  texture.    90  inches. 


^y  11.  Irregularly  bedded  sandstone,  marked  with  iron.    22  Jnchos. 


Total  thickness,  10  feet  and  6  inches. 


1.  Earth. 

3.  Yellow  sandy  and  oolitic  magnesian  limestone.    18  inches. 


\V-.\Vv.V-.\V-.-.V    3.  Green  sandstone.    4  inches. 
^-g^Sr     4.  Oolitic  magnesian  limestone,  as  above.    33%  inches. 


5.  White  sandstone.    3  inches. 

6.  Oolitic  magnesian  limestone,  as  above.    9  inches. 

7.  Yellow  sandstone.    4  inches. 

8.  Sandy  silicious  limestone.    13  inches. 


rr    9.  Oolitic  layer.    3  inches. 
i-'v-i    10.  Sandy  and  Oolitic  limestone.    13  inches. 

f'.O^7';. -/:-.•:.    11.  Yellow  sandstone,  marked  with  green.    15  inches. 
Total  thickness,  8  feet  and  654  inches. 

The  increase  of  silicious  matter  in  the  latter  is  very  noticeable.  This  is  perhaps  due 
to  the  fact  that  the  ledge  from  which  the  section  is  taken  here  approaches  within  a  half 
mile  of  the  Archjean  outcrop  of  granite  in  this  town,  previously  described.  As  it  arose 
into  the  Lower  Magnesian  horizon,  it  might  perhaps  rationally  be  supposed  to  produce 


280 


GEOLOGY  OF  EASTERN  WISCONSIN. 


such  a  modification  of  the  limestone  in  its  vicinity.  But  the  fact  of  changeableness  ia 
nevertheless  a  general  one. 

Through  Hortonia  the  course  of  the  ledge  is  eastward,  in  which  direction  the  forma- 
tion slowly  dips,  until  in  the  town  of  Ellington  it  is  covered  by  the  St.  Peters  sand- 
stone and  Trenton  limestone,  which,  standing  out  in  a  similar  escarpment,  seem,  to 
form  a  continuation  of  the  Lower  Magnesian  ledge. 

It  has  already  been  remarked  that  the  course  of  the  streams  in  this  vicinity  is  peculiar. 
The  Wolf  river,  when  it  arrives  opposite  this  rock  banier,  turns  sharply  to  the  west, 
while  a  little  stream  traverses  the  township  of  Ellington  in  an  almost  direct  line  parallel 
to  this  ledge,  and  enters  the  Wolf  river  at  the  point  of  its  sudden  flexure.  This  little 
stream  lies  in  the  level  bottom  of  a  valley  averaging  about  a  mile  in  breadth.  On  its 
south  side,  in  sections  25  and  26  of  the  town  of  Ellington,  highly  fossiliferous  limestone 
of  the  Trenton  period  reaches  from  near  the  flood  plane  of  the  valley  upwards,  35  feet  or 
more.  On  the  opposite  side  of  the  valley,  in  section  24,  there  arises  from  the  same  flood 
plane,  a  mural  cliff  of  Lower  Magnesian  limestone  to  the  height  of  more  than  50  feet. 
The  accompanying  figure  presents  the  relations  of  these  formations: 

FIG.  34. 


1.  Potsdam  sandstone.    2.  Lower  Magnesian  limestone.    3.  St.  Peters  sandstone. 
4.  Trenton  limestone. 

The  rock  forming  this  Lower  Magnesian  cliff  is  a  very  hard,  silicious  dolomite,  of 
almost  flinty  texture,  striking  fire  readily  from  impact  of  the  hammer,  and  yielding  a 
resonance  and  fracture  more  like  quartzite  than  ordinary  limestone.  Its  distant  bedding 
joints  are  very  obscure,  in  the  main  body  of  the  cliff,  while  irregular  vertical  fissures  are 
numerous  and  conspicuous.  Geodes  of  limpid  and  opalescent  quartz  are  scattered  through 
it.  These  characteristics  pertain  in  full  only  to  the  cliff  in  question.  To  the  east  a  low- 
er ledge  of  the  more  usual  coarse,  silicious  limestone  extends  some  distance  into  the  next 
township,  and  a  similar  ledge  on  the  west,  curves  to  the  north,  and  is  lost  under  the 
drift.  But  it  soon  reappears  and  extends  with  insignificant  interruptions  onward  to  the 
vicinity  of  the  Wok*  river.  The  strata,  like  those  on  the  south  side  of  the  valley,  rise  in 
that  direction,  so  that  near  the  river  the  upper  face  of  the  Potsdam  sandstone  is  brought 
considerably  above  the  flood  plane,  and  a  profile  section  across  the  valley  at  Stephens- 
ville  would  show  a  very  unequal  elevation  in  the  Lower  Magnesian  strata. 

Still  further  to  the  westward,  within  about  two  miles  of  New  London,  two  conspicu- 
ous mounds,  known  as  North  and  South  Musquito  Hill,  rise  about  200  feet  above  the  R, 
R.  grade  at  the  depot.  Their  main  mass  is  sandstone,  but  they  are  crowned  with  calca- 
reous strata.  On  the  western  brow  of  the  south  hill  the  uppermost  layers  exposed  are 
thin,  banded,  arenaceous  and  oolitic,  and  are  succeeded  below  by  two  feet  of  shelly,  rot- 
ten, mottled  layers,  underlaid  by  sixteen  inches  of  thin-bedded,  flag-like  rock,  under 
which  again  lies  a  foot  of  hard,  broken,  chippy  rock,  which  in  turn  rests  upon  quartzose 
sandstone  beds  of  6  inches  to  24  inches  in  thickness.  The  actual  exposure  of  the  sand- 
stone is  confined  to  a  few  feet,  but  the  precipitous  slope  indicates  its  presence  in  conside- 


LOWER  MAGNESIAN  LIMESTONE.  281 

rable  thickness.  On  the  south  face  an  exposure  exhibits  the  same  section,  with  some- 
thing' of  the  usual  tendency  to  variableness. 

On  the  north  hill,  near  the  crest,  a  quarry  has  been  opened  in  straw  colored,  calciferous 
strata,  whose  bedding,  as  exposed,  ranges  from  2  inches  to  12  inches  in  thickness.  Cer- 
tain layers  are  somewhat  greenish,  and  green  spots  abound  in  others.  The  slope  below 
affords  occasional  glimpses  of  gray  and  green  sandstones. 

It  may  be  stated  incidentally,  as  an  interesting  fact,  that  a  loose  block  of  Trenton  lime- 
stone was  found  on  the  summit  of  this  hill. 

The  character  of  the  inagnesian  limestone  reposing  on  the  summits  of  these  hills  dif- 
fers somewhat,  it  will  be  observed,  from  that  of  the  lower  beds  of  the  Lower  Magnesian 
limestone  on  the  opposite  side  of  the  Wolf  river,  and  may  not  belong  to  precisely  the 
same  horizon,  but  it  is  evident  that  it  cannot  belong  to  a  higher,  and  if  it  does  not  be- 
long to  the  same  geological  level,  must  constitute  an  intercalated  band  in  the  Potsdam 
sandstone.  But  the  elevation  of  the  junction  of  the  sandstone  and  limestone  on  Mus- 
quito  Hill  was  estimated  to  be  100  feet  higher  than  the  junction  of  the  sandstone  and 
limestone  on  the  opposite  side  of  the  valley.  It  appears  then  that  for  a  distance  of  about 
twenty  miles  (how  much  more  is  not  known),  the  formations  on  the  north  side  of  the 
valley  are  notably  higher  than  on  the  south  side.  While  it  is  possible  that  all  this 
may  be  due  to  a  southward  dip  of  no  great  magnitude  in  itself,  but  quite  unusual  in 
these  formations  in  this  region,  especially  in  that  direction,  it  seems  more  consonant 
with  all  the  facts  of  the  case,  to  suppose  that  tho  valley  represents  the  line  of  a  fault 
with  a  downthrow  on  the  south  side. 

It  is  in  this  region  that  the  stair-like  border  of  this  and  the  higher  formations  is  most 
conspicuous.  From  the  eastward-bearing  ledge  just  under  discussion,  the  western  limit 
oi  the  formation  runs  in  its  irregular  zigzag  way,  almost  due  north  to  Lake  Shawano, 
where  it  turns  again  nearly  due  east  along  the  south  side  of  the  Oconto  river. 

Passing  by  for  want  of  space  several  ledges  that  occur  in  the  towns  of  Black  Creek, 
Cicero,  Lesser  and  Hartland,  which  will  have  value  as  the  country  develops,  we  find  at 
the  angle  made  south  of  Lake  Shawano,  the  following  beds  forming  the  summit  of  a 
bluff  133  feet  high,  the  lower  portion  of  which  is  Potsdam  sandstone.  (Sec.  34,  S.  E.  qr., 
T.  27,  R.  16  E.) 

1.  Earth. 

2.  Rather  thin  bedded,  shaly  arenaceous  magnesian  limestone,  4  feet. 

3.  Bluish  irregular  magnesian  limestone,  containing  geodes  of  quartz,  3  feet. 

4.  Compact  silicious  limestone,  1  foot. 

5.  Grayish  white  magnesian  limestone,  8  niches. 

6.  Cherty  magnesian  limestone,  1  foot  and  6  inches. 

7.  Light  gray  magnesian  limestone,  3  feet. 

8.  Oolitic  layer,  2  feet. 

9.  Concealed,  3  feet. 

10.  Oolitic  layers,  3  feet. 

11.  Light  colored  magnesian  limestone,  partially  exposed. 

12.  Slope,  concealing  sandstone. 

At  Oconto  Falls  the  following  section  is  shown: 

1.  The  uppermost  portion  exposed  consists  of  grayish  buff,  silicious  dolomite,  of  me- 
dium hardness,  somewhat  uneven  texture,  being  in  part  minutely  granular  crystalline, 
and  in  part  earthy,  containing  frequent  cavities  varying  from  the  size  of  a  pea  to  that  of 
a  walnut.  These  cavities  are  sometimes  partially  lined  with  quartz  crystals,  but  these 
miniature  geodes  are  so  much  less  prevalent  than  in  the  layer  below,  which  is  studded 
with  them,  and  with  clusters  of  quartz  crystals,  as  to  make  this  a  distinguishing  feature. 
The  bedding  is  irregular,  but  as  exposed  in  the  face  of  the  gorge,  the  layers  are  from  one 


282  GEOLOGY  OF  EASTERN  WISCONSIN. 

foot  thick  downwards.    The  rock  weathers  to  a  granular,  sandy  surface,  much  pitted 
from  unequal  resistance  to  the  elements,  and  showing  lines  of  deposition,  o.l  feet. 

2.  A  group  of  beds  very  similar  to  the  above,  but  characterized  by  a  much  greater 
abundance  of  crystalized  quartz,  lining  the  numerous  small  cavities,  or  forming  small 
clusters.    There  is  no  distinct  line  of  demarkation  between  these  and  the  above  layers. 
11.7  feet. 

3.  Below  the  above  lies  a  thick  bed  of  impure  conglomeritic  dolomite,  the  component 
fragments  having  an  almost  flinty  hardness  and  fracture.     It  presents  the  appearance 
of  having  been  formed  of  fragments  of  silicious  dolomite  imbedded  in  a  matrix  of  dolo- 
rnitic  sand  and  mud,  which  afterwards  cemented,  and  in  a  measure,  coalesced.     On 
weathering,  the  constituents  are  brought  out  conspicuously.    The  more  compact  frag- 
ments seem  to  contain  a  considerable  percentage  of  silica  disseminated  through  them, 
while  segregations  of  quartz,  much  oftener  in  the  crystalline  than  the  nodular  form,  are 
very  numerous,  and,  standing  out  upon  the  weathered  surface,  give  it  a  very  rough  as- 
pect.   This  layer  by  its  hardness  offers  great  resistance  to  erosion  from  the  volume  of 
water  pouring  over  it,  but  when  undermined  by  the  removal  of  the  softer  rock  below, 
it  falls  in  huge  masses,  sometimes  20  feet  in  maximum  diameter,  which  lie  in  the  chan- 
nel for  ages  before  complete  removal.    The  prevailing  color  of  the  rock  is  dark  gray, 
mottled  by  the-whitp  quartz,  and  the  variously  colored  fragments  of  which  it  is  composed. 
The  thickness  of  the  bed  is  varying,  that  measured  as  an  average  being  4 . 7  feet. 

4.  Underlying  the  above  is  a  very  hard,  impure  dolomite  of  a  dark  gray  color,  mottled 
•with  lighter  hues,  and  of  more  uniform  texture  than  that  above,  but  still  not  homogene- 
ous, while  some  portions  are  studded  with  small  geodes  and  clusters  of  quartz  crystals. 
It  is  not  subdivided  into  regular  beds,  but  is  much  fissured  vertically.     9.7  feet. 

5.  Still  lower  lies  a  stratum  of  less  hardness,  much  finer  and  more  uniform  crystalline 
grain,  and  more  distinctly  laminated,  so  as  to  present  a  horizontally  banded  appearance. 
It  has  a  bluish  gray  cast  on  the  fresh,  somewhat  conchoidal  fracture,  distantly  stained 
with  dark  purplish  brown  iron  spots,  but  weathers  to  a  dirty  gray.    The  quartz  segrega,- 
tions  descend  from  above  into  the  upper  layers  of  this.    4.7  feet. 

An  analysis  of  this  stratum  by  Mr.  G.  Bode  gave: 

Carbonate  of  lime 49.414 

Carbonate  of  magnesia 39.784 

Silica 7 . 638 

Alumina 1 .473 

Oxide  of  iron 1 .691 


100.000 

6.  Below  this  follows  a  bed  of  green  and  purple  shale  and  argillo-arenaceous  dolomite, 
having  the  following  composition: 

Carbonate  of  lime 29.370 

Carbonate  of  magnesia 18.860 

Silica 37.798 

Alumina 9.621 

Oxide  of  iron 4. 351 


100.000 

This  shale  very  closely  resembles  that  of  the  Eureka  section,  and  probably  belongs  to 
the  same  horizon.  It  is  to  the  softness  of  this  shale  and  the  ease  with  which  it  is  eroded, 
that  the  falls  are  due.  2  feet. 


LOWER  MAGNESIAN  LIMESTONE.  283 

7.  A  yellowish  or  grayish  dolomite  of  very  rough,  irregular,  granular  crystalline  and 
earthy  texture,  containing  geodes  and  almost  devoid  of  bedding  lines.  6  feet. 

S.  At  the  base  of  the  above,  are  two  thin  layers  that  present  a  virescent  hue,  caused 
by  small  green  spherules  imbedded  in  a  gray  rock.  Associated  with  these  are  a  greater 
or  less  number  of  oolitic  spherules,  some  ocherous,  and  others  in  which  the  center  is  yel- 
low and  the  exterior  green,  which  suggests  that  the  coloring  matter  may  be  a  ferrous 
compound  of  iron  which  oxidizes  to  the  hydrated  ferric  form.  On  the  weathered  portion 
of  the  rock  these  little  spherical  bodies  are  wholly  or  partially  dissolved  out,  giving  a  harsh, 
minutely  pitted  surface.  Those  that  are  partially  dissolved,  show  a  radiating  structure 
somewhat  resembling  some  of  the  Foraminifera,  but  the  rays  are  not  reducible  to  any 
definite  numerical  system.  Aggiegations  of  similar  problematic  forms,  not  green,  but 
usually  white,  occur  in  and  upon  the  surface  of  the  layers,  disposed  precisely  as  the 
white  oolitic  masses  are  in  the  layers  below,  some  of  which  show  clearly  a  concretionary 
structure,  making  it  probable  that  all  are  so.  They  deserve  more  study  than  it  has  been 
possible  yet  to  give  them.  The  same  layers  contain  many  illy  preserved  remains  of 
what  appear  to  be  an  undescribed  species  of  Salterella  and  also  an  undetermined  Gas- 
teropod  having  a  low  broad  coil.  The  gray  portion  of  the  rock  is  a  mixture  of  earthy 
and  crystalline  granular  material,  rather  soft,  and  has  an  easy  regular  fracture.  6  inches. 

9.  This  fossiliferous  layer  graduates  below  into  a  very  peculiar  dolomitic  and  silicious 
rock,  in  which  the  concretionary  structure  attains  an  unusual  development.    Almost  the 
whole  mass  is  formed  of  vanously  sized  concentric  segregations  of  chtrt  and  dolomitic 
material.    They  are  not  unfrequently  two  or  three  feet  in  diameter,  and  resemble  coarse, 
gigantic  Stromatopora.   2.2  feet. 

10.  This  rests  upon  a  dark  gray  dolomite,  similar  to  that  immediately  above  the  con- 
cretionary layer,  but  contains  aggregated  masses  of  white  oolite,  and  is  itself  somewhat 
oolitic  from  the  presence  of  yellowish  and  dark  gray  spherules.    The  white  ones  are  of 
large  size,  and  upon  fracture  and  abrasion  show  their  con  centre  structure.    They  are 
aggregated  so  as  to  form  flat  or  nodular  masses  similar  to  those  usually  assumed  by  chert 
in  this  and  the  higher  Silurian  formations.     16  inches. 

11.  Closely  associated  with  this  below  is  a  layer  of  a  pistachio-green  cast  formed  by 
abundant  green  spots,  with  which  are  mingled  a  less  number  of  yellow,  orange  and  red- 
dish ones,  the  rock  mass  being  gray.    Aside  from  the  colored  spherules,  it  is  slightly 
oolitic  and  rather  soft,  possessing  a  regular  easy  fracture.    The  Salterella  occurs  here 
also.    ?>  inches. 

12.  The  base  of  the  exposure  is  formed  by  a  dark  gray,  very  impure,  and  for  the  most 
part  oolitic  dolomite.    The  ooliths  are  generally  darker  than  the  mass  of  the  rock,  and 
the  larger  ones  are  seldom  perfectly  spherical,  but  incline  to  the  forms  usually  assumed 
by  chert  nodules.    Ocherous  spherules  occur,  and  occasionally  red  hematite  ones.    In 
some  layers,  quartzose  sand  is  abundant,  forming  seams  or  lenticular  masses.     Geodes, 
both  of  quartz  and  calcite  occur.    The  bedding  is  very  irregular.    5  fe  t. 

Total  exposure.  53.2  feet. 

The  falls  have  a  vertical  descent  of  22  feet,  with  a  fall  of  10  feet  on  the  rapids  above, 
and  a  greater  amount  balow. 

A  few  miles  north  of  Stiles,  on  Jones  creek,  a  thinner  band  of  shale,  very  similar  to 
that  described  above,  gives  rise  to  a  diminutive  imitation  of  Oconto  Falls,  though  the 
layers  are  not  specifically  identifiable  with  those  of  the  preceding  section.  The  dip  is 
undulating,  so  that  though  shown  for  some  distance  along  the  stream,  but  a  small  verti- 
cal thickness  is  exhibited. 

The  upper  portion  of  the  formation  is  displayed  at  several  points  between  Angelica 
and  the  Oconto  river;  at  Ordway's  ledge  and  vicinity,  about  five  miles  north  of  Stiles; 
and  on  the  south  side  ot  the  main  Peshtigo  river,  from  above  the  mouth  of  the  Little 
river  to  near  the  bend  above  Potato  rapids.  At  these  several  points  the  uneven  nature 


284  GEOLOGY  OF  EASTERN  WISCONSIN. 

of  the  superior  face  of  the  formation  is  shown  to  be  still  a  prominent  fact.  The  last 
mentioned  point  is  120  miles  from  that  at  which  this  feature  was  first  described,  show- 
ing that  this  is  not  a  local  or  exceptional  character,  but  one  that  attaches  to  the  forma- 
tion throughout  this  portion  of  the  state,  and  to  some  extent,  at  least,  beyond. 

As  the  formation  passes  across  the  Menomonee  river  into  Michigan,  it  affords  us  ;; 
parting  glimpse  at  the  Grand  Rapids.  The  section  is  closely  similar  to  that  at  Oconto 
Falls,  and  will  not  be  here  repeated.  A  full  description  is  given  by  Dr.  Rominger  in  his 
report  on  the  Paleozoic  Rocks  of  the  Upper  Peninsula  of  Michigan,  p.  72. 

Economic  Considerations.  —  Many  portions  of  this  formation  fur- 
nish stone  well  suited  for  heavy  masonry,  as  locks,  piers,  founda- 
tions, etc.  Its  heavy  beds,  somewhat  silicious  character,  and  free- 
dom from  shaly  matter,  render  it  enduring,  while  it  is  wrought  with- 
out difficulty.  Other  portions  are  adapted  to  ordinary  construction, 
and  exceptional  portions  are  fitted  for  cutting. 

The  rock  is  burned  at  numerous  points  for  quicklime,  and  when  a 
judicious  selection  is  made,  which  is  not  always  the  case,  with  good 
results.  The  mass  of  the  formation  is  not  adapted  to  this  purpose,  but 
some  parts  are  exceptionally  pure  dolomites,  and  properly  burned,  pro- 
duce a  most  excellent  lime.  Selection  becomes  a  matter  of  much  im- 
portance, and  as  it  is  equally  BO  with  other  formations,  and  other  por- 
tions of  the  state,  the  volume  on  the  general  geology  of  the  state  will 
contain  specific  information  and  directions  that  will  assist  in  choosing 
a  suitable  stone. 

Some  of  the  less  pure  portions  produce  a  lime  that  forms  a  slightly 
hydraulic  mortar,  suitable  for  general  construction,  but  whose  infe- 
rior whiteness  reduces  its  value  for  finishing  purposes.  In  some  cases, 
where  the  rock  is  burned  at  a  low  heat,  the  hydraulic  property  be- 
comes sufficiently  marked  to  be  very  serviceable  in  many  cases  where 
common  quicklime  will  not  answer,  and  where  the  more  expensive 
cement  is  too  costly.  I  am  informed  by  Hon.  "Win.  Starr,  of  Ripon, 
that  formerly,  lime  of  this  class  from  the  Lower  Magnesian  limestone 
at  that  place  was  used  for  cisterns  with  success,  and  that  in  removing 
the  foundations  of  a  mill  that  had  stood  many  years  exposed  to  water, 
the  mortar  made  from  this  lime  was  found  in  excellent  condition. 

An  analysis  of  the  rock  which  constitutes  a  portion  of  one  of  the 
mounds  previously  described,  taken  from  the  N.  W.  J  of  the  K.  E.  \ 
of  Sec.  20,  Ripon,  gave  the  following  result: 

Carbonate  of  lime 51 . 68 

Carbonate  of  magnesia ! . . .  40.93 

Sesquioxide  of  iron 0-60 

Alumina , 8.09 

Silica 3.16 

Water 0 . 70 

100.16 


ST.  PETERS  SANDSTONE.  285 

Insoluble  in  acids,  6.17  per  cent.,  or  nearly  the  entire  amount  of 
silica  and  alumina. 

Messrs.  Blish  &  Barlow  manufacture  a  hydraulic  lime  from  rock 
belonging  to  this  formation,  found  in  the  X.  "W.  J  of  Sec.  26,  town  of 
Poygan,  Winnebago  county. 

The  following  analysis  by  Prof.  "W.  "W.  Daniells,  shows  it  to  be  an 
impure  dolomite: 

Carbonate  of  lime 49 . 747 

Carbonate  of  magnesia 38 . 189 

Insoluble  in  acid 9.442 

Sesquioxide  of  iron  and  alumina 1 . 587 

Water..                                                                                              ....  1.190 


The  insoluble  residue  consisted  of  silica,  5.803,  and  alumina,  3.639. 
The  manufactured  product  is  used  in  the  vicinity,  and  in  the  neigh- 
boring cities. 

Some  of  the  argillo-arenaceous  dolomites,  associated  with  the  shale 
belt  of  this  formation,  have  a  composition  approaching  very  near  that 
of  some  of  the  well  known  cement  rocks  of  the  country,  as  will  be 
seen  by  reference  to  the  analysis  of  Layer  6,  at  Oconto  Falls,  previ- 
ously given,  which  was  made  with  this  fact  in  view,  and  which  de- 
serves consideration,  though  the  stratum  at  that  point  is  unfavorably 
situated. 

ST.  PETERS  SANDSTONE. 

Upon  the  billowy  surface  of  the  Lower  Magnesian  limestone,  filling 
up  its  troughs,  and  in  most  cases  surmounting  the  crests  of  its  prom- 
inences, lies  the  St.  Peters  sandstone.  This  formation  has  usually 
been  described  as  a  very  uniform  deposit  of  purely  quartzose,  inco- 
herent, pebbleless,  non-fossiliferous  sandstone.  All  these  characteris- 
tics fail  in  eastern  Wisconsin. 

Owing  to  tne  unequal  surface  of  the  Lower  Magnesian  limestone  pre- 
viously described,  its  thickness,  instead  of  being  remarkably  uniform, 
is  precisely  the  opposite.  It  is  known  to  vary  within  the  district  un- 
der description  from  two  hundred  and  twelve  feet  down  to  a  single 
layer  of  sand  grains.  It  ranges  from  zero  to  one  hundred  feet  or 
more  —  within  a  quarter  of  a  mile,  in  one  case,  at  least,  and  changes 
in  a  similar  rapid  and  remarkable  manner  at  many  other  points.  In 
the  instances  of  its  entire  disappearance,  its  thickness  is  not  sufficient 
to  overtop  the  prominences  of  the  lower  formation,  and  the  Trenton 
limestone  above  rests  directly  upon  the  Lower  Magnesian  limestone. 


286  GEOLOGY  OF  EASTERN  WISCONSIN. 

while  in  the  immediate  vicinity,  observed  depths  of  sandstone  of  fifty- 
four  feet,  eighty-two  feet,  and  one  hundred  feet  have  been  noted. 
This  irregularity  appears  to  be  greatest  from  Dodge  county  north- 
wards. In  the  southern  part  of  the  district,  and,  so  far  as  the  Artesian 
wells  enable  us  to  judge,  in  the  lake  shore  region,  a  greater  degree  of 
uniformity  prevails.  In  other  words,  the  unevenness  of  the  Lower 
Magnesian  surface  seems  to  have  been  greatest  ^ear  its  margin,  or 
near  the  shore  line  of  the  ocean  at  the  time  of  its  deposit;  and  as  it 
recedes  to  the  eastward  and  southward,  it  becomes  more  uniform. 

Setting  aside,  for  the  moment,  a  large  number  of  exceptional  cases, 
arising  chiefly  from  the  foregoing  peculiarities,  the  rock  may  be  de- 
scribed essentially  as  it  is  found  to  be  elsewhere,  being  composed  of 
well  rounded,  rather  uniform,  transparent,  incoherent  grains  of  quartz, 

forming  a  very  friable  rock. 
Calcareous  and  argillaceous 
matter  are  almost  entirely  ab- 
sent. White,  yellow  and  gray 
are  the  most  prevalent  colors, 
but  red,  brown,  pink  and 
green  are  not  uncommon. 
Sometimes  the  rock  is  beauti- 
fully variegated  and  in  other 

SHOWING  COLORATION  OF  ST.  PETERS  SANDSTONE  AT    ^aSCS    »"   1S     Danued    in    a    U1S- 

RlFON-  jointed    and    irregular   way, 

The  shaded  portion  represents  brown  sandstone;  the    nrodnfMno-   a  vprv'intprpstincr 
remaining  portion  is  white,  lined  and  flecked  with  pink.    " 

and  unique  effect.  This  is 

imperfectly  illustrated  in  the  accompanying  figures.  In  the  upper 
part  of  the  formation,  irregular  concretions  of  iron  ore  occur,  which, 
on  weathering,  present  a  dark  brown,  glazed  surface,  which  leads  to 
the  popular  impression  that  they  are  of  volcanic  or  meteoric  origin. 

In  structure,  the  St.  Peters  sandstone  is  finely  laminated,  fre- 
quently in  oblique  and  cross  lines,  and  shows  at  some  points  fine  ex- 
amples of  ebb  and  flow  structure.  The  bedding  is  usually  obscure. 
Vertical,  oblique  and  irregular  fissures  frequently  traverse  the  forma- 
tion, cutting  it  into  huge,  irregular  masses. 

The  exceptions  to  these  general  characteristics  arise  chiefly  from 
the  relation  of  this  sandstone  to  the  irregularities  of  the  underlying 
formation.  Where  it  adjoins  the  sloping  sides  of  the  limestone 
mounds,  it  has  derived  from  them  ingredients  not  possessed  else- 
where. More  or  less  of  calcareous  matter  would  necessarily  become 
mingled  with  the  sand  during  its  deposit.  The  amount  observed  is 
not  so  great  as  might  be  expected,  and  sandstone  within  a  few  feet  of 


ST.  PETERS  SANDSTONE.  287 

limestone  clipping  under  it  at  an  angle  of  25°,  and  rising  thirty  feet 
above  it,  has  been  observed  to  be  almost  perfectly  free  from  calca- 

reous  matter.  It  is  to  be  re- 
marked, however,  that  the 
arching  form  of  these  lime- 
stone mounds,  and  the  con- 
I  centric  nature  of  the  external 
layers  are  most  admirably 
adapted  to  resist  erosion,  and 

SHOWING  THE  COLORATION  OF  ST.  PETERS  SANDSTONE    that  by  the  nearness   of   these 

domes    to    each   other,    they 

would  afford  mutual  protection  from  violent  wave  action.  Conglom- 
eritic  and  brecciated  rock,  formed  by  fragments  of  the  limestone  im- 
bedded in  the  sandstone,  have  been  observed  at  several  points,  but 
only  in  very  close  relation  to  the  limestone. 

A  much  more  prevalent  modification,  especially  to  the  northward, 
consists  of  thin  seams  of  white  argillaceous  material  interlaminated 
with  the  sand  and,  to  some  extent,  diffused  through  it,  giving  it  a 
schistose  character.  It  then  possesses  considerable  coherence,  and  is 
found  in  large  firm  masses  on  the  slope  below  the  ledges  of  Trenton 
limestone.  At  some  points,  ferruginous  matter  mingles  with  the  cal- 
careous and  argillaceous  ingredients,  forming  a  variegated  rock  not 
unlike  the  red  and  purple  shales  of  the  Mendota  beds. 

In  addition  to  the  modifications  arising  from  the  Lower  Magnesian 
limestone,  the  Archaean  rocks  contribute  others,  which  have  perhaps 
been  sufficiently  described  in  connection  with  the  quartzites  of  Port- 
land and  "Waterloo. 

At  several  points  in  Hock  county,  the  passage  of  the  St.  Peters  to 
the  formation  above  is  attended  by  an  alternation  of  sandstone  and 
calcareous  rock.  The  sandstone  just  below  the  calcareous  bed  is 
marked  with  fucoidal  impressions  and  the  base  of  the  calcareous  layer  • 
contains  abundant  Scolithus  tubes.  The  calcareous  bed  is  of  a  green- 
ish gray  cast  containing  a  large  percentage  of  insoluble,  argillo-arena- 
ceous  material,  in  addition  to  the  evident  quartzose  grains  ihat  are 
more  or  less  freely  scattered  through  portions  of  it.  This  has  not 
been  observed  to  attain  a  thickness  of  more  than  four  or  five  feet. 
The  upper  portion  is  usually  shaly  and  appears  at  some  points  to 
have  been  eroded  before  the  deposition  of  the  stratum  of  sandstone 
above.  This  latter  is  thin  and  mixed  with  argillaceous  material  on 
which  sometimes  supervenes  a  thin  seam  of  carbonaceous  matter  fol- 
lowed by  the  fossiliferous  Trenton  limestone.  At  the  most  northern 
point  at  which  the  junction  was  seen,  the  sand  mingles  freely  with 


283  GEOLOGY  OF  EASTERN  WISCONSIN. 

the  calcareous  layers  of  the  Trenton,  for  several  feet  above  their  base. 
At  most  other  points  the  usual  abrupt  transition  was  observed. 

Organic  Remains.  Previous  to  the  present  year  (1876)  there  has 
been  no  published  announcement  of  the  existence  of  fossils  in  this 
formation.  In  the  Fourth  Annual  Report  of  the  Geological  Survey 
of  Minnesota,  Prof.  IS".  II.  Winchell  describes  a  Lingulepis,  found 
near  Fountain  in  that  state,  in  the  upper  beds  of  the  formation. 

In  my  unpublished  report  of  1873,  Scolithus  borings  were  de- 
scribed as  occurring  in  rock  in  the  town  of  Waterloo,  referred  to  the 
St.  Peters  sandstone.  In  1874,  this  was  confirmed  "by  finding  well 
preserved  tubes  of  the  same  in  the  town  of  JBeloit,  in  strata  belonging 
to  the  upper  part  of  the  formation.  Fucoidal  impressions  were  also 
found  at  the  same  locality.  In  1875,  Scolithus  tubes  were  seen  in. 
sandstone  referred  doubtfully  to  the  base  of  the  formation. 

In  a  synopsis  of  my  report  for  these  years,  three  hundred  copies  of 
which  were  printed  and  distributed  at  private  expense,  in  the  early 
part  of  January,  1876,  the  existence  of  organic  remains  in  this  for- 
mation was  announced.  This  form  of  announcement  will  not  proba- 
bly be  regarded  as  sufficient  to  justify  a  claim  to  priority,  in  this  in- 
teresting discovery.  The  organic  remains  so  far  have  been  found  ex- 
clusively where  the  sandstone  was  compacted  by  some  cementing  ma- 
terial, which  justifies  the  belief  that  the  absence  of  fossils  throughout 
the  greater  part  of  the  formation  is  due  to  want  of  preservation  and 
not  to  original  absence  of  life  in  the  depositing  sea. 

Method  of  formation.  The  existence  of  the  remains  of  marine 
life  demonstrates  that  the  fossiliferous  portions  at  least  are  submarine 
deposits,  while  the  well  rounded  character  of  the  grains,  the  ebb  and 
flow  structure,  the  shaly  laminations,  the  conglomeritic  portions  and 
its  relations  to  the  adjacent  formations  leave  no  doubt  that  it  belongs 
to  the  common  class  of  oceanic  sand  deposits. 

Extent  and  Local  Descriptions.  The  St.  Peters  sandstone  enters  this  district  from 
Illinois  and  from  the  Lead  Region  at  the  southwestern  corner  of  Rock  county.  Owing 
to  the  ease  with  which  the  sandstone  is  eroded,  it  usually  occupies  only  a  narrow  belt 
close  under  the  protecting  ledges  of  the  overlying  Trenton  limestone,  and  appears  on 
the  map  as  a  narrow  border  to  that  formation.  In  some  places,  as  in  Rock  county, 
where  it  is  represented  as  occupying  more  ample  areas,  it  is  quite  probable  that  if  the 
drift  could  be  removed  the  sandstone  would  be  found  absent  at  some  points.  The  pre- 
glacial  rivers  undoubtedly  cut  entirely  through  it,  but  their  position  cannot  now  be  ac- 
curately mapped. 

In  Rock  county  it  may  be  readily  identified,  since  it  seldom  shows  itself  except  under 
a  protecting  shelf  or  crown  of  Trenton  limestone,  whose  characteristic  fossils  are  easily 
recognized,  and  by  the  simpler  fact,  that  it  is  the  only  sandstone  exposed  in  the  county. 
Its  upper  portion  is  amply  displayed  in  the  western  portion  of  the  county,  where  the 
drift  is  light,  but  presents  so  great  similarity  that  it  will  be  unnecessary  to  enter  into 


ST.  PETERS  SANDSTONE.  289 

local  details.  A  feature  occurs  in  the  north  part  of  the  township  of  Magnolia,  of  this 
c  -unty,  deserving  notice.  A  small  stream,  known  as  Allen's  creek,  flows  westward 
along  the  line  separating  sections  4, 5,  and  6,  on  the  north,  from  sections  7,  8  and  9,  on  the 
south.  On  each  side  there  is  a  range  of  bluffs  capped  with  Trenton  limestone  and  under- 
laid with  St.  Peters  sandstone.  The  junction  of  the  two  formations  on  the  south  side 
is,  by  aneroid  measurement,  155  feet  above  the  stream,  and  on  the  opposite  side,  in  sec- 
tion 6,  32  feet,  showing  a  difference  of  123  feet.  This  superior  elevation  of  the  south 
bluft'is  maintained  as  far'to  the  east  as  the  two  can  be  compared.  In  section  7,  about 
midway  between  the  two  bluff's,  there  is  a  very  sharp  east  and  west  ridge  of  hard  sand- 
stone, intersected  in  every  direction  by  a  network  of  silicious  seams  that  stand  out  prom- 
inently on  the  weathered  surface,  as  though  the  rock  had  been  extensively  fractured  and 
subsequently  reunited  by  silicious  cement.  This  ridge  rises  50  feet  above  the  junction 
of  St.  Peters  and  Trenton  on  the  north  side  of  the  stream.  These  fact*  are  illustrated 
by  the  accompanying  figure. 

FIG.  37. 


SHOWING  THE  RELATIONS  OF  THE  ST.  PETERS  SANDSTONE  AND  TBENTON  LIMESTONE,  MAGNOLIA. 

In  this  quiet  region  of  gentle  southeastward  dips,  these  phenomena  are  unusual, 
though  insignicant  in  general  geology.  They  are  equally  explainable  by  supposing  a 
flexure  of  the  strata  or  a  fault. 

At  the  railroad  cut  near  Magnolia  station,  the  transition  from  the  St.  Peters  sand- 
stone to  the  Trenton  limestone  is  well  shown.  The  main  cut  consists  of  the  limestone, 
the  lower  3  or  4  feet  of  which  are  more  or  less  sandy.  Below  this  lies  8  inches  of  sandstone 
containing  seams  and  nodules  of  iron  oxide  and  sulphide,  doubtless  all  originally  pyrites. 
This  layer  of  sandstone  rests  upon  4  feet  4  inches  of  impure  sandy  conglomeritic  linie- 
rock,  full  of  Scolithus(?)  tubes.  Below  this,  continuing  to  the  base  of  the  exposure,  is 
an  incoherent  sandstone,  mottled  and  banded  with  yellow,  orange  and  green  colors,  and 
exhibiting  oblique  and  horizontal  lamination.  A  similar  transition  may  be  seen  at  nu- 
merous other  points  in  Rock  county.  From  this  county  onward,  the  general  course  of 
the  formation  is  due  north  for  about  sixty  miles,  and  then  east  of  north  for  more  than 
one  hundred  miles.  Its  irregularity  of  thickness  in  tracing  it  northward  first  becomes 
pronounced  in  the  western  part  of  Dodge  county,  and  it  is  first  known  to  be  entirely 
cut  off  by  the  contact  of  the  limestones,  below  and  above,  in  the  southern  part  of  Green 
Lake  county,  notwithstanding  which,  and  frequent  subsequent  interruptions,  it  main- 
tains an  existence  for  more  than  120  miles  to  the  northward.  It  was  last  observed  within 
about  four  miles  of  the  Michigan  line,  where  it  had  a  thickness  of  20  feet.  Beyond  that 
point  it  is  concealed  by  the  drift. 

The  formation  is  not  recognized  at  all  in  the  recent  geological  report  of  Michigan, 
although  the  foregoing  facts  offer  a  strong  presumption  that  it  exists  there.  Under  the 
impression  that  has  formerly  prevailed  concerning  the  uniformity  of  this  deposit,  the 
finding  of  the  Trenton  limestone  on  the  Escanaba  river,  resting  directly  upon  the  Lower 
Magnesian,  would  justify  the  inference  that  the  St.  Peters  sandstone 'was  essentially 
wanting  in  the  Upper  Peninsula  of  Michigan,  but  with  the  light  now  possessed,  the  fact 
of  contact  at  that  point  has  little  significance  in  relation  to  the  question  of  the  presence 
or  absence  of  the  formation  in  question. 
Wis.  SUR.  — 19 


290  GEOLOGY  OF  EASTERN  WISCONSIN. 

Economic  Considerations.  The  greatest  prospective  value  of 
this  formation  is  doubtless  its  water-bearing  capacity,  it  being,  as  has 
already  been  shown,  the  great  source  of  Artesian  fountains  in  this 
portion  of  the  state.  In  view  of  this  fact,  the  foregoing  developments 
in  respect  to  its  nature  possess  eminent  practical  importance. 

For  some  years  geologists  have  habitually  recommended  the  sand 
of  this  formation  for  the  manufacture  of  glass.  Its  value  for  that 
purpose  is  now  being  put  to  the  practical  test.  A  factory  has  recently 
been  established  at  Omro  for  that  purpose.  The  sand  is  derived  from 
near  Waukau.  A  six  pot  furnace  has  been  erected  having  a  capacity 
per  month  of  800  boxes  of  100  feet  each.  At  present  the  manufacture 
is  confined  to  window  glass  and  shades.  The  results  thus  far  attained 
are  reported  as  highly  satisfactory. 

In  the  town  of  Waterloo  the  sandstone  has  sufficient  compactness 
to  serve  as  a  building  stone,  but  usually  it  is  too  soft.  This  latter  fact, 
however,  permits  its  extensive  use  as  sand  for  mortar,  and  similar 
purposes.  At  most  localities  it  can  be  dug  with  pick  and  shovel,  the 
mere  handling  being  sufficient  to  reduce  it  to  sand.  On  account  of 
its  cleanness  and  sharpness,  it  is  much  superior  to  most  drift  sand. 

TRENTON  GROUP. 

Upon  the  St.  Peters  sandstone  there  lies  an  extensive  series  of  lime- 
stones and  shales,  which  represent  the  Trenton  period.  It  consists  of 
three  main  divisions,  which  are  recognized  in  geological  history  as 
epochs.  The  lowest  member  is  known  as  the  Trenton  limestone,  the 
next  in  order  as  the  Galena  limestone,  and  the  uppermost  as  the  Cin- 
cinnati shales  and  limestone.  These  are  firmly  linked  together  by  fos- 
sils common  to  the  three  horizons,  and  in  the  northeastern  part  of  the 
state  it  is  exceedingly  difficult  to  discern  any  satisfactory  line  of  de- 
markation  between  them.  In  the  southern  portion,  however,  they  are 
well  distinguished,  and  will  receive  consideration  in  the  order  named. 

O  ' 

TRENTON  LIMESTONE. 

Subdivisions.  The  Trenton  limestone  proper,  as  it  is  developed 
in  the  southern  portion  of  the  district  under  consideration,  consists  of 
four  subdivisions  sufficiently  well  characterized  to  be  valuable  aids  in 
the  study  and  discussion  of  the  formation,  and  in  the  practical  appli- 
cation of  the  results  of  the  survey. 

Adhering  as  closely  as  the  nature  of  the  case  will  admit,  to  the 
terms  already  in  use,  these  will  be  distinguished  as  follows: 


TRENTON  LIMESTONE. 


291 


FIG.  38. 


I • • 

I.     UPPER  BLUE  BEDS,  thickness,  15  feet. 


II.     UPPER  BUFF  BEDS,  thickness,  55  feet. 


III.     LOWER  BLUE  BEDS,  thickness,  25  feet. 


IY.     LOWER  BUFF  BEDS,  thickness,  25  feet. 


It  has  been  customary  to  divide  the  Trenton  limestone  of  this  state 
into  the  "  Buff  limestone  "  and  the  "  Blue  limestone,"  and  in  the  Lead 
region  the  latter  and  some  higher  beds  form  the  "  Glass  rock,"  "  Brown 
rock,"  and  "  Green  rock."  These  latter  terms  are  based  upon  litho- 
logical  characters  that  do  not  prevail  in  southeastern  "Wisconsin,  and 
hence  the  use  of  these  terms  would  be  undesirable  even  if  their  appli- 
cation within  the  Lead  region  was  sufficiently  well  defined  to  justify 
their  extension  to  other  localities. 

To  continue  the  unmodified  use  of  the  terms  Blue  and  Buff  lime- 
stone, and  to  rest  with  this  twofold  subdivision,  is  open  to  serious 
objection,  as  experience  has  shown. 

In  the  first  place,  ike  color  distinction  made  between  the  two  is 
not  applicable  without  qualification,  since  more  than  half  of  the  up- 
per portion  usually  designated  Blue  limestone  is  quite  as  persistently 
buff  as  the  lower  division.  The  unleached  interior  of  the  thicker 
beds,  in  all  the  subdivisions,  is  blue,  and  that  was  doubtless  the  origi- 
nal color  of  the  whole  formation,  but  the  two  divisions  designated  in 
tliis  report  as  Buff  are  habitually  leached  to  much  greater  depths 
than  the  remaining  two,  and  are  less  associated  with  bluish  green 
shales,  which  give  to  the  latter  a  bluish  or  greenish  aspect.  Applied 
as  now  suggested,  the  terms  blue  and  buff  become  reasonably  appro- 
priate and  very  convenient. 

In  the  second  place,  the  chemical  distinction,  viz. :  that  the  lower 
division  is  a  dolomite,  and  the  remainder  a  limestone,  does  not  hold 
good.  An  analysis  of  drippings  from  unweathered  layers,  represent- 
ing the  whole  thickness  of  what  has  heretofore  been  called  Buff  lime- 


292  GEOLOGY  OF  EASTERN  WISCONSIN. 

stone,  and  is  now  called  the  Lower  Buff  beds,  exclusive  of  the  argil- 
laceous layers  at  the  base,  shows  36.41  per  cent,  of  carbonate  of 
magnesia.  A  similar  analysis  of  the  Lower  Blue  beds  shows  38.39 
per  cent,  of  carbonate  of  magnesia.  A  like  analysis  of  the  lower 
13  feet  of  the  Upper  Buff  beds  gives  43.30  per  cent,  of  magnesic  car- 
bonate, and  one  of  a  higher  stratum,  34.86  per  cent.  These  analyses 
were  all  made  from  rocks  whose  exposure  to  leaching  and  weathering 
was  as  nearly  as  possible  equal,  and  from  adjacent,  where  not  identi- 
cal, localities,  all  being  from  the  vicinity  of  Beloit. 

From  these  it  appears  that  the  quantity  of  magnesia  varies  but 
slightly,  and  that  the  entire  amount  is  large,  so  that  the  term  dolo- 
mite is  applicable  here  as  well  as  to  the  calcareous  formations  above 
and  below,  while  the  Blue  limestone  of  the  Lead  region  is  a  true  lime- 
stone, containing  but  little  magnesia. 

In  the  third  place,  the  paleontological  distinction  heretofore 
drawn  does  not  hold  good.  The  Buff  limestone  has  been  regarded  as 
characterized  by  great  numbers  of  Gasteropoda,  Cephalopoda  and 
Lamellibranchiata,  especially  by  species  referable  to  Tellinomya, 
Cypricardites  and  allied  genera.  But  this  is  at  least  equally  true  of 
the  Upper  Buff  beds  of  this  report. 

The  following  species  catalogued  in  the  report  of  1862,  as  belonging 
to  the  Lower  Buff  limestone,  have  been  found  in  the  Upper  Buff  beds 
of  this  report: 

Cypricardites  Niota,  C.  rotundatus,  C.  ventricosus,  Modiolopsis 
superba,  Tellinomya  nasuta,  T.  ventricosa,  Murchisonia  helicteres, 
Pleurotomaria  (Raphistoma)  N~asoni,  P.  subconica,  Trochonema, 
umbilicatum,  Raphistoma,  lenticular  is,  Cyrtoceras  annulatuw^  C. 
eugium,  Oncoceras  Lycus,  O.  Pandion  and  0.  plebium. 

Only  one  of  the  list  given  in  the  report  of  1862  as  from  the  Buff 
is  known  to  me  as  occurring  exclusively  in  the  Lower  Buff,  while 
three  have  been  found  in  the  Upper  Buff  that  have  not  been  observed 
in  the  Lower.  The  majority  are  common  to  the  two  subdivisions, 
and  to  this  number  several  allied  species  have  now  been  added. 
Coltimnaria  alveolata,  also  regarded  as  peculiar  to  the  Lower  Buff,  is 
found  in  the  upper  beds. 

The  strata  at  Rockton,  which  belong  to  the  Upper  Buff  beds,  are 
referred  to  the  Buff  limestone  of  previous  authors,1  and  a  similar  par- 
donable confusion  of  the  two  members  has  undoubtedly  been  ex- 
perienced by  other  writers  on  the  geology  of  this  region. 

These  facts  are  dwelt  upon  to  this  extent  to  demonstrate  the  ne- 
cessity for  the  introduction  of  a  new  classification,  and  of  new  terms 

1  See  pp.  89,  90,  Vol.  V,  Geol.  Rep.  of  111. 


TRENTON  LIMESTONE.  293 

in  lieu  of  those  that  have  already  found  a  place  in  the  literature  of 
M'estern  geology. 

It  is  not  presumed  that  the  distinctions  here  made  have  any  wide 
geographical  application,  and  hence  the  terms  in  common  use  have 
only  received  such  qualification  as  the  geology  of  this  region  demands. 

The  term  beds  has  been  substituted  for  limestone,  since,  in  tha 
opinion  of  the  writer,  these  divisions  do  not  rise  to  the  dignity  of 
what  are  technically  known  among  geologists  as  epochs,  to  which 
grade  the  more  significant  term  should  be  confined,  unless  there  are 
special  lithological  reasons  for  its  use  otherwise.  While  it  is  very 
much  in  the  interests  of  science,  and  its  practical  application,  to  sub- 
divide the  several  formations  as  far  as  the  facts  will  permit,  and  thus 
give  to  our  discriminations  and  descriptions  as  much  of  exactness  as 
possible,  much  confusion  is  introduced  into  the  general  literature  of 
the  science,  if  each  of  these  minor  members  is  clothed  with  a  formal 
title. 

/.  The  Lower  Buff  Beds.  It  has  already  been  observed  in  connec- 
tion with  the  St.  Peters  sandstone,  that  a  slight  alternation  of  sand- 
stone and  calcareous  layers  occurs  in  the  transition  to  the  Trenton 
limestone,  there  being  above  the  main  body  of  sandstone  a  calcar- 
eous layer  of  about  four  feet  thickness,  overlaid  by  a  bed  of  sand- 
stone two  feet  or  less  in  thickness.  Above  this  there  follow  the 
Lower  Buff  beds.  Their  usual  thickness  is  from  eighteen  to  twenty- 
five  feet.  At  some  points  the  formation  seems  to  be  made  up  of 
three  main  strata,  the  lower  one,  more  or  less  shaly  toward  the  bot- 
tom, of  about  four  feet  thickness,  the  middle  one  seven  feet,  and  the 
upper,  twelve.  These  are  less  distinctly  subdivided  into  beds  from 
two  feet  in  thickness  downwards.  "When  these  distinctions  are  not 
observable,  the  layers  are  of  a  similar  heavy  bedded  character,  except 
when  affected  by  the  action  of  the  elements.  The  texture  is  some- 
what irregular,  arising  from  an  uneven  association  of  earthy  and 
crystalline  material.  The  general  aspect  is  earthy,  but  crystalline 
particles  compose  the  greater  part  of  the  mass.  The  color,  as  seen  in. 
natural  ledges  and  superficial  quarries,  is  a  light  yellowish'buft'  or 
gray.  The  interior  of  thicker  and  less  exposed  layers  frequently  has 
a  bluish  cast. 

The  rock  is  composed  of  carbonate  of  lime  and  magnesia,  a  con- 
siderable percentage  of  silicious  and  aluminous  material,  and  an  in- 
significant ingredient  of  iron  and  the  more  common  salts.  Crystals  of 
calcite  and  occasionally  those  of  pyrite  occur  in  cavities. 

The  fossils  of  this  division  are  abundant,  although  less  so  than  in 
the  upper  divisions,  especially  the  blue  beds. 


29-4  GEOLOGY  OF  EASTERN  WISCONSIN. 

The  following  is  a  partial  list  of  the  species  that  lived  during  the 
deposition  of  these  strata: 

Buthotrephis  succulens,  Streptelasma  (Petraia)  corniculum,  a  new 
species  of  Stictopora  and  one  of  Trematopora,  a  Lingula,  resembling 
L.  obtusa,  Orthis  disparalis,  O.perveta,  0.  subquadrata,  O.  tricenaria, 
Streptorhynchus  deflectum,  S.filitextum,  8.  dettoideum,  /S.  planum- 
lonum,  Strophomena  alternata,  S.  camerata,  S.  camura,  S.  incras- 
sata,  a  new  species  of  Hhynchonella,  Tellinom.ya  nasuta,  Cypricar- 
dites  Canadensis,  C.  rectirostris,  C.  -rotundatus,  C.  subtruncatus, 
C.  ventricosus,  C.,  n.  sp.,  Modiolopsis  superba,  Ilelicotoma  planu- 
lata,  Raphistoma  lenticularis,  R.  Nasoni,  Pleurotomaria  subconica, 
Trochonema  arribiguum,  T.  umbilicatum,  Murchisonia  tricar india, 
M.  bicincta,  Subulites  elongatus,  Bucania  bidorsata,  Bellerophon 
bilobatus,  Pterotheca  attenuata,  Orthoceras  anellum,  O.junceum,  O. 
vertebrale,  O.,  n.  sp.,  0.  Beloitense,  Oncoceras  Pandion,  0.  plebeium, 
Gyroceras  convolvans,  Lituites  occidentalis,  Illcenus  taurus,  Cer- 
aurus  pleurexanthenws  and  Leperditiafabulites. 

It  is  impossible  in  the  present  state  of  our  knowledge  to  name  any 
single  fossil  of  common  occurrence  that  is  peculiarly  characteristic 
of  this  geological  horizon  The  abundance  of  Lamellibranchiates, 
Gasteropods  and  Cephalopods,  and  the  fewness  of  the  Corals  and  Bry- 
ozoans  sufficiently  distinguish  it  from  both  of  the  Blue  beds  above, 
but  not  from  the  Upper  Buff  beds  to  which  this  division  bears  a  strong 
resemblance  paleontologically  as  well  as  lithologically.  At  some 
points  the  Lower  Buff  beds  develop  something  of  a  shaly  character  at 
the  base,  and  are  highly  fossiliferous,  in  which  cases  the  facies  of  the 
fauna  strongly  resembles  that  of  the  Blue  beds,  which  are  likewise 
shaly.  It  appears  from  all  the  facts  that  there  was  an  alternation  of 
conditions  in  the  depositing  Trenton  seas,  and  that  when  the  condi- 
tions were  such  as  to  favor  the  formation  of  limestone  simply,  the  life 
above  characterized  predominated,  and  that  whenever  the  conditions 
changed  so  as  to  cause  a  deposit  of  shale  interleaved  with  layers  of 
limestone,  the  brachiopodous  and  coralline  fauna  prevailed.  These 
subdivisions  then  signify  rather  physical  mutations  of  a  more  or  less 
local  nature,  than  wide  spread  changes  in  the  life  -character  of  the  period. 

2.  The  Lower  Blue  Beds.  The  upper  surface  of  the  preceding  di- 
vision is  at  most  points  well  defined,  and  upon  its  thick  beds  rest  an 
alternating  series  of  thin,  impure  limestone  layers  and  thinner  shaly 
leaves.  These  are  usually  grouped  into  more  massive  beds,  and  where 
removed  from  the  action  of  surface  agencies,  the  shaly  portions  often 
possess  sufficient  coherence  to  bind  the  limestone  layers  into  beds  of 
respectable  dimensions. 


TRENTON  LIMESTONE.  295 

The  average  thickness  may  be  put  down  at  from  twenty  to  twenty- 
five  feet.  The  limestone  is  varying  in  texture.  Usually  it  is  a  mix- 
ture of  earthy  material  and  minute  crystals,  but  sometimes  has  a 
compact  crystalline  structure,  and  occasionally  a  coarse  granular  one. 
Some  layers  are  little  else  than  a  mass  of  fossils.  The  color  is  bluish, 
or  grayish,  weathering  to  light  gray  or  buff. 

The  shale  is  a  bluish  green,  and  aside  from  mingling  with  the  lime- 
stone somewhat,  it  forms  seams  and  partings  between  the  layers. 
These  are  seldom  over  two  inches  thick  in  the  southern  part  of  our 
province,  but  attain  more  considerable  dimensions  at  the  north.  A 
notable  amount  of  carbonaceous  material  is  sometimes  associated  with 
this  shale.  It  is  usually  very  highly  fossiliferous. 

In  chemical  composition  the  limestone  layers  do  not  essentially 
differ,  so  far  as  tested,  from  the  Buff'  already  described,  being  an  im- 
pure magnesian  limestone.  The  analysis  previously  referred  to  in- 
cluded only  the  limestone  layers,  the  shaly  partings  being  excluded. 
Including  these,  probably  one-third  of  the  whole  mass  would  be  found 
to  be  silicious  and  aluminous  material. 

Besides  the  bluish  green  cast  that  the  shale  gives  to  the  mass,  it  has 
served  to  protect  the  limestone  from  the  leaching  action  of  percolat- 
ing water,  so  that  it  also  oftener  retains  its  original  bluish  hue  than 
the  beds  below  and  above,  and  renders  the  name  applied  to  it  not  in- 
appropriate. It  is  characterized  by  a  much  greater  abundance  of  fos- 
sils than  the  beds  below.  These  differ  from  those  below  in  the 
much  greater  abundance  of  Corals,  Bryozoans  and  small  Brachio- 
pods,  especially  the  Orthidse.  Murchisonia  gracilis  appears  in 
great  abundance  near  the  base  of  this  division.  It  is  not  found  in 
my  somewhat  extensive  collections  from  the  Lower  Buff,  which  indi- 
cates its  rarity,  though  perhaps  not  absence,  from  that  horizon.  Bel- 
lerophon  ~bilobatus  is  very  abundant,  though  not  confined  to  this 
horizon.  This  division  comprehends,  in  greater  or  less  numbers,  a 
large  proportion  of  all  the  species  found  in  the  Trenton  limestone  of 
this  region. 

j.  The  Upper  Buff  Beds.  This  is  the  thickest  and  most  important 
subdivision  of  the  group  in  the  Rock  river  valley,  reaching  a  vertical 
dimension  of  fifty-five  feet.  It  is  less  uniform  in  its  several  parts 
than  the  two  preceding,  and  is  less  easily  described  in  general  terms, 
and  the  reader  will  perhaps  find  the  detailed  description  of  the  sec- 
tion at  Beloit,  given  subsequently,  under  the  head  of  local  descrip- 
tions, more  satisfactory  than  the  general  statements  here  made.  The 
most  prevalent  kind  of  rock  is  a  rather  heavy  bedded  limestone,  ob- 
scurely banded  and  mottled  with  light  gray  and  buff,  giving  the 


296  GEOLOGY  OF  EASTERN  WISCONSIN. 

whole  a  liglit,  yellowish,  buff  aspect.  The  gray  portions  are  more 
compact  and  crystalline  than  the  buff,  which  are  porous  and  earthy 
although  beautifully  bespangled  with  glistening  crystalline  facets. 
These  characters  apply  more  particularly  to  the  lowest  and  uppermost 
members;  the  latter  is  distinguished  by  the  presence  of  nodules  of 
chert.  A  portion  of  the  intermediate  layers,  while  retaining  some- 
thing of  the  nature  above  described,  becomes  much  more  irregular  in 
texture,  and  possesses  a  very  rough  fracture,  which  gives  the  ledges 
in  the  quarry  a  brecciated  appearance  that  is  increased  by  the  pres- 
ence of  cavities. 

Another  portion  is  more  homogeneous  in  structure  than  either  of 
the  preceding  kinds,  and  has  a  very  noticeable  conchoidal  fracture, 
resembling  in  this  respect  the  glass  rock  of  the  Lead  region,  from 
which,  however,  it  differs  in  having  a  less  compact  and  more  earthy 
texture,  caused  by  the  presence  of  from  12  to  15  per  cent,  of  alumin- 
ous and  silicious  material.  It  is  lined  with  obscure  reddish  stains, 
probably  of  fucoidal  origin.  This  constitutes  two  bands,  two  to  four 
feet  thick,  lying  near  the  center  of  the  division  and  separated  seven 
or  eight  feet  from  each  other.  They  thus  constitute  reliable  laud- 
marks  in  correlating  partial  exposures  at  distant  points,  and,  if  intel- 
ligently used,  will  prove  a  serviceable  guide  to  the  quarryman. 

The  life  at  this  stage  was,  as  has  been  remarked,  very  similar  to 
that  at  the  time  of  the  deposit  of  the  Lower  Buff  beds,  but  was  more 
prolific  and  varied.  Nearly  sixty  species  are  known  to  occur  in  these 
beds,  and  it  is  presumable  that  the  actual  number  is  much  larger. 

Of  these,  between  fifteen  and  twenty  have  not  been  found  in  the 
Lower  Buff  beds,  but  until  more  thorough  search  has  been  made  it 
would  not  be  wise  to  regard  them  as  diagnostic.  The  occurrence  of 
Halysites  at  this  horizon  is  especially  worthy  of  remark,  as  being  the 
lowest  point  at  which  it  has  yet  been  authentically  reported  in  the 
western  series. 

4.  The  Upper  Blue  Beds.  These  are  so  similar  in  general  charac- 
ter to  the  Lower  Blue  Beds,  as  not  to  need  extended  description. 
They  differ  from  them  chiefly  in  those  cases  where  they  take  on  a 
coarse  granular  character,  approaching  that  of  the  Galena  limestone 
above,  to  which  they  constitute  the  transition.  The  degree  in  which 
they  are  thus  modified  varies  with  the  locality.  At  several  points 
there  are  only  four  or  five  such  transitional  beds,  and  at  other  points 
the  whole  division  shows  something  of  this  character. 

An  abundance  of  Brachiopods,  Bryozoans  and  Chcetetoid  corals 
form  the  leading  feature  of  the  life  of  this  period.  Its  general  .aspect 
is  more  manifestly  similar  to  that  of  the  Cincinnati  shales  above  the 


TRENTON  LIMESTONE. 


FIG.  39. 


Galena  than  that  of  the  beds  below.     Leptwna  sericea  is  a  very  abun- 
dant fossil,  which  has  not  been  observed  to  be  true  below. 

Local  Descriptions.  In  the  vicinity  of  Beloit  are  a  number  of  natural  and  arti- 
ficial exposures  that  are  so  fortunately  situated  at  different  elevations  as  to  exhibit  tho 
entire  thickness  of  the  formation,  and  yet,  an  equally  fortunate  cir- 
cumstance for  the  students  of  geology  of  that  locality,  their  correct 
correlation  is  attended  with  something  of  difficulty,  and  is  only  ac- 
complished by  careful  and  industrious  study.  By  combining  tho 
partial  series  shown  at  the  various  points,  the  following  general 
section  for  that  vicinity  may  be  constructed: 

UPPER  BLUE  BEDS. 

A.  A  greenish  blue  impure  limestone,  chiefly  earthy  and  sub- 
crystalline,  but  in  part  granular,  beds  thin  and  separated  with 
shale,  very  fossiliferous.    Estimated  thickness,  fifteen  feet. 

UPPER  BUFF  BEDS. 

B.  I.  In  general  a  fine  grained,  impure  limestone,  of  earthy  or 
subcrystalline  texture,  the  former  a  light  buff', the  latter  gray,  com- 
bined so  as  to  give  an  obscure  banded  and  mottled  appearance 
quite  peculiar.    Nodules  of  chert  are  present,  which  distinguish 
it  from  the  rock  below.    Beds,  thick  and  uniform,  fracture,  easy  and 
regular  in  the  upper  two-thirds,  while  that  of  the  lower  part  is 
very  rough  and  angular,  as  though  from  a  brecciated  structure; 
more  impure  than  the  upper  portions.    A  shaly  layer,  7  feet  froci 
the  base,  contains  carbonaceous  seams  with  Graptolite  markings. 
Twenty-two  feet. 

II.  Layer  of  homogeneous  structure,  conchoidal  fracture,  and 
earthy  texture,  but  sparkling  with  minute  crystals;  lined  and  spot- 
ted with  obscure  reddish  fucoidal  stains.    Two  and  one  half  feet. 

III.  Combines  to  some  extent  the  character  of  the  layers  above, 
being  less  homogeneous  than  the  last,  and  more  so  than  the  pro- 
ceding.    Some  layers,  very  fossiliferous,  the  remains  being  grouped 
more  or  less  in  colonies.     Horizon  of  the  Halysites.    Seven  to  eight, 
feet. 

IV.  Similar  to  II,  but  the  characters  more  marked.    Three  to 
four  feet. 

V.  Similar  to  I,  but  not  cherty.    Texture  toward  the  upper  part 
more  irregular  than  below.    Nineteen  feet. 

LOWER  BLUE  BEDS. 

C.  Thin-bedded  impure  limestone  of  varying  earthy  and  crys- 
talline texture,  interleaved  with  shaly  partings,  the  whole  having 
a  bluish-green  or  gray  color.    Very  fossiliferous.    Twenty-three 
feet. 

LOWER  BUFF  BEDS. 

D.  Thick-bedded,  buff  limestone,  of  rather   coarse   texture, 
somewhat  shaly  at  the  base.    Fossils  not  very  abundant  except  in 
the  shaly  portions,    Twenty-three  feet. 

Transitional  layer  of  sandstone,  2  feet. 
Transitional  layer  of  impure  limestone,  4  feet. 
St.  Peters  sandstone. 
St.  p. 


298  GEOLOGY  OF  EASTERN  WISCONSIN. 

At  Clute's  point,  near  the  east  line  of  Sec.  10,  town  of  Beloit,  about  four  miles  north  of 
the  city,  the  upper  portion  of  the  St.  Peters  sandstone  and  the  lower  part  of  the  calcare- 
ous transition  bed  is  shown.  About  a  quarter  of  a  mile  southeast  of  this,  in  Sec.  11,  N, 
W.  qr.  of  S.  W.  qr.,  the  transition  stratum  is  better  shown,  tog-ether  with  the  layer  of 
sand  above  and  the  bottom  layers  of  the  Lower  Buff  beds.  About  an  equal  distance 
further  south,  near  the  high  bluff  that  overlooks  the  river,  cherty  layers,  B,  I,  and  a  por- 
tion of  those  above  are  shown.  The  latter  partake  quite  decidedly  of  the  characteristics 
of  the  Galena  limestone,  and  are  less  shaly  than  usual.  Passing  over  the  high  hill  to  a 
ravine  on  its  southwest  flank,  the  Galena  limestone  and  some  of  the  upper  transitional 
layers  may  be  found.  Nearly  a  mile  further  south,  at  the  large  quarry  near  the  C.  & 
N.  W.  R.  R.,  a  portion  of  the  St.  Peters  sandstone,  the  calcareous  transitional  layer,  the 
mterstratified  layer  of  sand,  the  shaly  layers  of  the  Lower  Buff  limestone,  one  of  which 
is  especially  crowded  with  Leperditiafabulites,  the  heavy  Lower  Buff  beds  in  full,  and  the 
Lower  Blue  beds,  may  be  seen  in  magnificent  vertical  exposure. 

A  partial  analysis  of  chippings  from  the  entire  thickness  of  the  Buff  and  Blue  layers 
at  this  point,  exclusive  of  the  thin  ones  at  the  base,  shows  the  following  composition: 

Buff.  Blue. 

Insoluble  residue.., 5.74  10.29 

Soluble  silica 1 .96  1 .75 

Sesquioxide  of  iron  and  alumina 3.27  1 .60 

Carbonate  of  magnesia 36 .40  38.39 

Carbonate  of  lime,  etc.,  by  estimate 52.63  47.97 


Total 100.00        100.00 


In  a  ravine  a  little  south  of  this  the  upper  part  of  the  Lower  Buff  and  the  lower  part 
of  the  Lower  Blue  beds  are  shown  in  a  small  quarry.  Still  further  south  along  the  rail- 
way, another  large  quarry  exhibits  a  considerable  portion  of  the  Lower  Buff  and  Bluo 
beds,  and  below,  near  the  track,  the  St.  Peter  sandstone  is  slightly  exposed.  Several 
minor  openings  along  this  line  of  bluffs  display  limited  sections.  A  mile  or  more  to  the 
southeast,  at  Carpenter's  quarry,  on  the  line  between  sections  26  and  27,  the  lower  por- 
tion of  the  Upper  Buff  beds  —  B.  V,  IV,  III  and  a  portion  of  II,  of  the  preceding  sec- 
tion —  are  extensively  wrought,  the  lower  beds  especially  being  a  desirable  building- 
stone.  The  ravine  below  this  quarry  has  gullied  into  the  Lower  Blue  beds,  and  show.s 
their  character  wherever  subjected  to  the  full  action  of  atmosphere,  frost,  and  water. 

A  partial  analysis  of  the  strata  B.  V  and  B.  IV,  at  Carpenter's  quarry,  shows  their 
chemical  nature  to  be  as  follows : 

,— Upper  Buff.—-, 
B.  IV.         B.  V. 

Insoluble  residue 12.50  3.42 

Soluble  silica 1.87  1.99 

Sesquioxide  of  iron  and  alumina 2.23  1 .42 

Carbonate  of  magnesia 34.86          43.87 

Carbonate  of  lime,  etc.,  by  estimate 48.54         49.30 

Total 100.00        100.00 


A  mile  and  a  half  farther  southwest,  Hess1  quarry  appears  to  lie  across 
marked  B.  II,  in  the  section,  and  to  include  some  of  the  layers  above  and  below,  tiiu 
latter  being  especially  prolific  in  fossils  heretofore  classified  as  characteristic  of  the  Buff. 
At  Hanchett's  quarry,  a  short  distance  south  of  this,  the  present  exposure  reaches  from 
about  three  feet  below  the  bed  marked  B.  IV,  to  about  the  top  of  B.  II.  A  little  over 


TREXTON  LIMESTONE. 


299 


a  half  mile  northwest  of  this  point,  at  Smith's  quarry,  the  junction  of  the  Upper  Blue 
beds  and  the  Galena  limestone  with  a  few  feet  above  and  below  is  shown,  completing 
the  series.  This  junction  may  also  be  seen  between  Turtleville  and  Shopiere. 

The  quarries  at  Rockton,  Illinois,  present  a  magnificent  section  of  the  Upper  Buff  beds 
from  layer  B.  IV  upwards  to  the  lower  portion  of  the  Upper  Blue  beds . 

These  statements  are  given  thus  specifically  that  there  may  be  the  fullest  opportunity 
for  verifying  and  utilizing  the  statements  of  this  report,  and  that  there  may  hereby  be 
furnished  a  basis  for  the  more  accurate  study  of  the  vertical,  and,  to  some  extent,  hori- 
zontal range  of  the  exceedingly  interesting  fossils  of  these  beds,  which  it  is  hoped  will 
be  prosecuted  by  the  geologists  of  the  region.  A  series  of  collections  carried  on  for  years 
under  the  favorable  opportunities  afforded  by  continuous  quarrying,  in  which  the  exact 
locality  and  horizon  should  be  carefully  noted,  could  not  fail  to  show  valuable  results. 

Over  one  hundred  species  of  fossils  are  known  to  occur  in  these  beds,  among  which  the 
following  identifications  have  been  made : 


Buthotrephis  succulens. 
Steptelasma  corniculuni. 
Cha3tetes  lycoperdon. 
Cha^tetes  discoideus. 
Stictopora  elegantula. 
Stictopora,  n.  sp. 
Schizocrinus  nodosus. 
Ptilodictya  recta. 
Lingula,  sp.  und. 
Orthis  perveta. 
Orthis  plicatella. 
Orthis  testudinaria. 
Orthis  pectinella. 
Orthis  tricenaria. 
Orthis  bellarugosa. 
Strophomena  camerata. 
Strophomena  alternata. 
Strophodonta,  sp.  und. 
Streptorhynchus  deflectum. 
Streptorhynchus  subtentum. 
Leptsena  sericea. 
Rhynchonella,  sp.  und. 
Ambonychia  attenuata. 
Ambonychia,  n.  sp. 
Ambonychia  lamellosa. 
Cypricardites  Niota. 
Cypricardites  rotundatus. 
Cypricardites  ventricosus. 
Cypricardites,  n.  sp. 
Tellinomya  nasuta. 
Tellinomya  alta. 
Tellinomya  Iphigenia. 
Tellinomya  levata. 
Tellinomya  ventricosa. 
Modiolopsis  superba. 
Modiolopsis  plana. 
Raphistoma  lenticularis. 


Raphistoma  Nasoni. 

Trochonema  ambiguuin. 

Trochonema  umbilicatum. 
j^R-ochonema  Beloitense,  n.  sp. 

Plurotomaria  subconica. 

Murchisonia  bicincta. 

Murchisonia  gracilis. 

Murchisonia  helicteres. 

Murchisonia  pagoda. 

Murchisonia  tricarinata. 

Cyclonema  percarinatum. 

Subulites  elongatus. 
j/Clisospira  occiclentalis,  n.  sp. 

IMicotoinu  planulata. 

Maclurea  Bigsbyi. 
,/Metoptoma  perovalis,  n.  sp. 

"elltTophon  bilobatus. 
ellerophon  Wisconsinensis,  n.  sp. 
jucama  JbueDi,  n.  sp. 

Bucania  punctifrons. 

Bucania  bidorsata. 

Pterotheca  attenuata. 

Baconi,  n.  sp.    •  —  - 


Gyroceras,  sp.  und. 
,£yrtoceras  annulatum. 

Cyrtoceras  corniculum. 

Cyrtoceras  eugium. 

Cyrtoceras  Neleus. 

Oncoceras  abr  upturn. 

Oncoceras  Alceus. 

Oncoceras  Lycus. 

Oncoceras  Pandion. 

Oncoceras  plebeium. 

Oncoceras,  sp.  undescribed. 

Oncoceras,  sp.  undescribed. 

Orthoceras  anellum. 
^jQrthoceras  nlulticameratum. 


300  GEOLOGY  OF  EASTERN  WISCONSIN. 

Orthoceras  junceum.  Worm  borings. 

Orthoceras  planoconvexum.  Illtenus  ovatus. 

Orthoceras  Beloitense.  Asaphus  Barrandi. 

Orthoceras  2  sp.  undes.  Asaphus  lowensis. 

Orthoceras  vertebrale.  Ceraurus  pleurexanthemus. 

l/13ndoceras  annulatum.  Encrinurus  sp.  undes. 

Endoceras  proteifonue.  Leperditia  fabulites. 
Gonioceras  anceps. 

In  the  vicinity  of  Janesville  are  a  number  of  extensive  quarries  and  natural  expo- 
sures that  display  the  three  lower  members  of  the  formation  quite  extensively.  At  the 
quarry,  a  mile  and  a  half  west  of  the  city  we  find,  at  the  base,  heavy  buff  layers,  con- 
taining but  few  fossils,  and  representing  the  Lower  Buff  beds.  The  complete  tliickness 
is  not  shown.  On  these  repose  thinner  bedded,  eminently  fossiliferous,  blue  and  gray 
beds  attended  with  shaly  layers  and  seams.  These  are  the  Lower  Blue  beds,  in  thick- 
ness, 22  feet  9  inches.  These  support  about  13  feet  of  light  buff  colored  limestone,  of 
uneven  structure  —  owing  to  earthy  or  soft  granular  spots  and  occasional  cavities  —  rather 
irregular  fracture,  giving  an  earthy  surface  with  crystalline  spangles,  and  containing 
but  few  fossils.  Beds  one  foot  or  less  in  thickness.  These  constitute  the  lower  portion 
of  the  Upper  Buff  beds.  The  following  species  were  observed  at  this  point,  nearly  all 
belonging  to  the  Blue  beds:  Bttthotrephis,  Chcetetes  lycoperdon,  Cr'moid  stems,  Stic- 
topora  (two  new  species),  Ptilodictya,  Trematopora,  Lingula  attenuata,  Orthis  perceta, 
0.  tricenaria.  0.  sp.  new  (like  0.  testudinaria),  Streptorhynchus  deflectum,  Strophomena 
camerata,  S.  incrassata,  Rhynchon-aella,  n.  sp.,  Ambonychia  lamellosa,  Tellinomya  n 
sitta,  Cypricardites  rotundatus,  C.  ventricosus,  Modiolopsis  plana,  Helicotomaplanulata, 
Raphistoma  lenticularis,  Trochonema  umbilicatum,  Murchisonia  helicteres,  M.  tricari- 
nata,  Pleurolomaria  subconica,  Bucania,  n.  sp.,  Pterotheca  attenuata,  Hyolithes  Baconi, 
n.  sp,,  Orthoceras  junceum,  0.  vertebrate,  0.,  n.  sp.,  Endoceras,  Proteif or  me,  Cyrtoceras 
Pandion?  Gomphoceras?  Asaphus  Barrandi,  I llctmus  ovatus,  Ceraurus  pleurexanthe- 
mus, Leperditia  fabulites  and  Beyrichia. 

At  the  lower  railroad  bridge  at  Janesville,  the  whole  of  the  Lower  Buff  limestone  is 
shown  resting  upon  the  St.  Peters  sandstone,  and  overlaid  by  about  30  feet  of  the  higher 
beds,  which  are  here  less  fossiliferous  than  usual.  A  section  of  this  exposure  is  given  in 
the  report  of  1862.  About  two  miles  above  the  city,  Eock  river  cuts  through  the  lower 
part  of  the  formation  and  into  the  St.  Peters  sandstone,  and  a  ravine  coming  in  on  the 
east,  through  which  the  road  ascends  from  the  river,  exposes  a  large  part  of  the  higher 
strata,  so  that  by  combining  the  sections,  nearly  the  whole  of  the  series  may  be  studied. 
Fossils  are  abundant  in  the  usual  layers. 

Farther  up  the  river,  above  Fulton  Center,  the  lower  strata  crown  the  bluffs  with 
weather-worn  outliers,  while  nearer  the  water's  edge  the  St.  Peters  sandstone  discovers 
itself.  They  become  somewhat  cavernous  at  one  point,  a  rare  feature  in  this  region. 
The  following  fossils  were  collected  along  the  ledges  on  the  west  side  of  the  river: 
Ch(etetes,  Streptelasma  corniculum,  Stictopora,  n.  sp.,  Orthis  pen-eta,  0.  tricenaria, 
Streptorhynchus  deflectum,  Strophomena  camerata  ?  S.  incrassata,  Rhynchonella,  Telli- 
nomya  nasuta,  Cypricardites  Canadensis,  C.  rectirostris,  C.  rotundatus,  C.  ventricosus, 
Modiolopsis  superba,  Raphistoma  lenticularis,  Trochonema  ambiguum,  Pleurotomaria 
subconica,  Murchisonia  tricarinata,  Bucania  tidorsata,  Pterotheca  attenuata,  Orthoceras 
junceum,  0.  vertebrale,  Ormoceras,  Illcenus  taurus,  Leperditia  fabulites. 

The  lower  beds  are  also  exposed  at  the  outlet  of  Lake  Koshkonong.  In  the  west- 
ern part  of  Rock  county  there  are  numerous  outcroppings  of  this  formation,  most  fre- 
quently of  the  lower  beds;  but  occasionally  also  of  the  higher  ones.  The-railway  cut 
near  Magnolia  station  exposes  the  Lower  Buff  beds,  and  furnishes  an  excellent  oppor- 


TRENTON  LIMESTONE.  301 

tunity  for  studying  its  character  and  fauna,  which  is  very  similar  to  that  already  given. 
The  uppermost  layers  of  the  Trenton,  and  its  junction  with  the  Galena  limestone  above, 
may  be  seen  satisfactorily  in  the  N.  E.  %  °f  Sec.  31,  and  in  the  S.  E.  ^  of  Sec.  19, 
town  of  Union,  where  a  new  species  of  Stictopora.  and  one  of  Trematopora,  Ptilodictya 
recta,  Orthis  perveta,  O.testudinaria,  0.  tricenaria,  Lcptwna  sericea,  and  Ceraurus  pleu- 
rexanthenius  indicate  the  character  of  a  fauna  very  abundant  in  individuals,  though  not 
especially  so  in  species.  At  the  lower  quarry  belonging  to  Mr.  Krump  near  Ft.  Atkin- 
son, the  upper  portion  of  this  formation  is  again  shown,  though  the  layers  are  some- 
what lower  than  the  above.  About  two  miles  below  Jefferson,  on  the  west  side  of  Rock 
river,  a  little  stream  has  cut  down  to  dark  mottled,  fine  grained,  rather  thick  beds  that 
are  capable  of  receiving  an  excellent  polish.  Their  lithological  affinities  are  with  the 
upper  half  of  the  formation. 

Near  Aztalan  are  several  quarries  showing  the  junction  of  the  Lower  Buff  layers  and 
those  above.  The  fossils  collected  were  chiefly  Buif  species.  The  surface  of  the  rock  is 
beautifully  polished  and  striated  by  glacial  action. 

On  the  north  side  of  Red  Cedar  Lake  in  the  town  of  Oakland,  and  in  the  vicinity,  on 
the  west,  the  lower  beds  are  displayed,  showing  a  somewhat  less  firm  rock  than  usual. 
The  first  mentioned  locality  affords  Schizocrinus,  Stictopora,  Orthis  perveta,  0.  plica- 
tella?  0.  tricenaria,  Streptorhynchus  felitextum,  Strophomena  incrassata?  Zygospira 
modesta?  Raphistoma  lenticularis,  Pleurotomaria,  Subulites  elongatus  and  Cyrtolites. 
To  which  the  others  add  Buthotrephis  succiiJens,  Strophomena  camerata,  Cypricardites 
rotundatus,  Orthocems  vertebrale,  Onnoceras  and  Gonioceras  anceps. 

The  most  interesting  exposure  of  the  Trenton  limestone  in  the  town  of  Waterloo  is 
at  the  quarry  of  Mr.  David  Crump  in  section  35.  The  lower  four  feet  are  of  thick  bedded, 
very  serviceable  rock,  above  which  lies  one  foot  of  thin  shaly  stone,  succeeded  by  six  feet 
of  somewhat  irregular  layers  of  medium  thickness,  upon  which  are  two  feet  of  even 
bedded  stone  overlaid  by  two  and  a  half  of  thin,  greenish,  shaly  material.  The  lower 
portion  is  to  be  regarded  as  representing  the  Lower  Buff  layers,  and  the  upper  ones 
the  Lower  Blue  limestone.  The  following  species  were  collected  in  a  limited  time  at 
this  locality:  Buthotrephis  succulens,  Graptolite-like  bodies;  Chcetetes,  Streptelasma 
corniculum,  Orthis  tricenaria,  Streptorhynchus  deflectum,  S.  planwribonum,  Stropho- 
mena incrassata,  a  new  species  of  Rhynchonella,  Tellinomya  ventricosa  (young)  Cyp- 
ricardites rotundotus,  and  a  new  species,  Raphistoma  lentieularis,  Pleurotomaria  sub- 
con  ica,  Murchisonia  bicincta,  M.  helictercs,  Orthoceras  annellum,  0.  vertebrale,  and  frag- 
ments of  Onnoceras  and  Cyrtoceras. 

The  Trenton  formation  outcrops  in  the  towns  of  Shields,  Portland,  Elba,  Lowell,  Cal- 
amus, Beaver  Dam,  Westford,  Fox  Lake  and  Trenton,  in  Dodge  county;  but  the  ex- 
posures in  all  cases  are  slight,  and  for  the  most  part  belong  to  the  base  of  the  formation. 
While  they  subserve  a  very  useful  purpose  in  supplying  their  respective  regions  with 
building  material,  they  add  little  to  our  knowledge  of  the  formation,  and  possess  but 
small  interest  to  the  geologist  or  general  reader. 

In  the  townships  of  Mackford  and  Green  Lake,  in  the  county  of  Green  Lake,  more 
frequent  and  extensive  exposures,  both  natural  and  artificial,  occur,  particularly  in  the 
vicinity  of  the  lakes  that  beautify  those  towns.  According  to  the  general  rule  already 
observed,  they  are  chiefly  the  lower  beds,  and  are  caused  to  stand  forth  by  the  easy 
degradation  of  the  sandstone  below. 

In  the  vicinity  of  Ripon  the  Lower  Buff  limestone  is  well  displayed.  One  of  the 
noticeable  peculiarities  in  this  neighborhood  is  the  unequal  elevation  of  the  base  of  the 
formation.  While  resting,  so  far  as  observed,  conformably  upon  the  St.  Peters  sand- 
stone, the  junction  is  found  at  varying  altitudes.  One  of  the  lowest  points  is  at  "  The 
Falls,"  within  the  city.  These  falls  are  caused  by  the  waters  of  Silver  creek  pouring 
over  the  lower  ledges  of  the  Trenton  limestone  and  excavating  the  softer  sandstone  be- 


302  GEOLOGY  OF  EASTERN  WISCONSIN. 

low.  By  following  up  the  stream,  a  strong  dip  to  the  north  of  east  may  be  observed. 
Fossils  are  not  abundant  here,  and  but  few  species  were  collected,  although  the  quarry- 
ing and  natural  exposures  afforded  ample  opportunities.  A  few  rods  west  of  the  busi- 
ness center  of  the  city,  the  lowest  layers  of  the  formation  are  about  40  feet  higher  than 
at  the  falls.  Along  the  bluff,  in  the  western  part  of  the  city,  the  same  layers  are  25  to 
30  feet  higher  still,  from  which  point  they  dip  to  the  south  until  they  disappear  beneath 
Crystal  creek  at  a  lower  point  than  that  at  which  they  occur  to  the  east  in  the  southern 
part  of  the  city.  To  the  west  of  this,  toward  Green  Lake,  the  base  of  the  formation  is 
more  nearly  horizontal.  In  section  5  of  the  township  of  Ripon,  about  three  miles  north- 
west of  the  city,  the  junction  in  question  occurs  at  a  lower  elevation,  if  an  aneroid  meas- 
urement is  to  be  trusted,  than  at  any  of  the  preceding  points. 

All  these  variations  may  be  readily  accounted  for  by  supposing  a  changeable  dip  of 
a  few  degrees;  but  they  are  nevertheless  unusual  in  this  formation.  As  the  floor  of  the 
formation  has  its  greatest  elevation  at  and  in  the  vicinity  of  the  point  where  it  rests 
upon  the  domes  of  Lower  Magnesian  limestone  previously  described,  and  has  a  lower 
elevation  as  it  recedes  from  this  point,  it  is  reasonable  to  suppose  that  the  phenomena 
may  be  due  to  that  relationship. 

The  following  species  representing  the  fauna  of  the  lower  beds  of  the  formation  were 
collected  in  this  vicinity,  the  quarries  of  Mr.  Coombs  and  Mr.  Corlis  proving  most  pro- 
lific :  Buthotrephis  succulens,  B.  gracilis,  Chcetetes,  Streptelasma  corniculurn,  Retepwa, 
Trematopora,  n.  sp.,  Lingula,  like  L.  obtusa,  Stictopora,  Orthis  perveta,  0.  tricenaria,  0. 
subquadrata,  Streptorhynchus  deflectum,  S.  deltoideum,  S.  filitextutn,  S.  planumbonum, 
Strophomena  alternata,  S.  camura,  S.  incrassata,  S.  tenuistriata,  Rhynchonella,  n.  sp., 
Tellinomya  nasuta,  Cypricardites  rotundatus,  C.  subtruncatus,  C.  ventricosus,  C.,  n.  sp., 
Modiolopsis  superba,  Helicotoma  planulata,  Raphistoma  lenticularis,  Trochonema  am- 
bigmim,  T.  umbilicatum,  Pleurotomaria  subconica,  Murchisonia  bicincta,  Holopea,  Siib- 
iiMes  elongatus;  Orthoceras  annellum,  0.  junceum,  0.  vertebrale,  0.  planoconwxum, 
0.,  sp.  new,  Cyrtoceras  (Oncoceras)  plebeium?  C.  Pandion,  C.  or  Gyroceras  (outer  cham- 
ber only),  Ormoceras,  Gyroceras  convolvans,  Lituites,  Illoenus  taurus,  Encrinurus,  Lep- 
erditia  fabu  lites,  Ceraurus  pleurexanthemus. 

North  of  Ripon,  the  formation  soon  becomes  doubly  covered  with  drift,  being  over- 
laid not  only  by  the  original  glacial  deposit  of  rubbish,  but  also  by  the  later  lacustrine 
clays,  and  hence  it  presents  itself  at  the  surface  even  more  rarely  than  before,  so  that 
our  attention  is  not  again  demanded  by  the  meager  and  scattered  exposures  until  we 
reach  the  vicinity  of  Neenah  and  Menasha,  where  a  cluster  of  interesting  quarries 
occur.  Leaving  out  of  consideration  those  directly  south  of  Neenah  and  north  of  Me- 
nasha, which  are  referred  to  a  higher  horizon,  we  find  a  belt  of  quarries  beginning  with 
Thompson's  in  Sec.  29,  Neenah,  and  extending  north  to  the  county  line,  which  possesses 
the  general  lithological  characters  of  the  Upper  Buff  beds,  which  have  already  been  ful- 
ly described.  The  following  list  of  species,  however,  collected  from  this  belt,  shows 
several  forms  not  observed  in  that  horizon  in  the  southern  part  of  the  state,  but  which 
are  common  in  a  higher  position  and  which  therefore  give  special  interest  to  the  fauna 
of  these  localities:  Two  new  species  of  Chcetetes,  Streptelasma  corniculum,  Columnaria, 
a  new  species  of  Stictopora,  Schizorinus  nodosus,  Lingula  quadrata?  Orthis  lynx,  0. 
plicatella,  0.  subquadrata,  0.  testudinaria,  0.  pectinella,  Streptorhynchus  deflectum,  S. 
filitextum,  Strophomena  alternata,  S.  incrassata,  S.  camerata,  Leptoena  sericea,  Zi/go- 
spira  recurvirostris,  Rhynchonella  Anticostensis,  Raphistoma  lenticularis,  Pleuroto- 
maria subconica,  a  new  species  of  Murchisonia,  having  a  lofty  spire,  Endoceras  pro- 
teiforme,  an  undetermined  Gyroceras  and  Leperdita  alia?  were  secured  in  the  limited 
time  that  could  be  devoted  to  collection. 

In  the  vicinity  of  Mr.  Verbeck's  residence,  near  the  southeast  corner  of  section  18, 
Menasha,  are  several  small  quarries  that  possess  interest  from  their  position  and  char- 


TRENTON  LIMESTONE.  303 

acter.  At  the  quarry  just  east  of  his  house,  the  rock  consists  of  thick  bedded,  light 
greenish  blue,  or  gray  limestone  containing  some  argillaceous  material  distributed 
through  the  mass  in  thin  leaves,  forming  a  rock  quite  similar  to  that  which  prevails  in 
the  bed  of  the  Lower  Fox  river.  Between  the  heavy  beds  are  greenish  blue  argilla- 
ceous shales  containing  fossils,  the  small  Brachiopods  of  the  Blue  beds  predominating. 

Opposite  this,  on  the  south,  a  few  feet  of  rock  of  a  similar  nature  but  more  fossilifer- 
ous,  are  underlaid  by  a  partially  exposed  bed  of  dark  blue  crystalline  rock.  About  forty 
rods  west  of  this  is  another  shallow  quarry  displaying  apparently  a  lower  horizon.  The 
mass  of  the  rock  here  has  a  rather  brittle,  compact,  crystalline  texture  of  dark,  slightly 
bluish  gray  color,  and  irregular  or  sometimes  vitreous  or  conchoidal  fracture.  In  tho 
lower  strata  there  is  much  chert,  distributed  in  layers  of  nodules  which  are  white  or  flint 
colored  and  fossiliferous.  The  rock  also  contains  frequent  small  geodes,  the  cavities  be- 
ing lined  with  calcite  and  occasionally  pyrite,  or  rarely  by  zinc  blende.  The  walls  of 
fissures  are  also  sometimes  lined  with  calcite  and  pyrite.  A  short  distance  to  the  nortli- 
vrest  of  the  quarry  first  mentioned  the  beds  present  the  more  usual  characteristics  of  the 
argillaceous  portions  of  the  Blue  limestone  as  seen  farther  south.  The  strata  at  these 
several  quarries  dip  at  an  angle  of  about  2°  to  the  southeast. 

Passing  on  to  the  north  about  ten  miles  we  find  in  the  S.  E.  qr.  of  section  28  of  the 
town  of  Center,  a  partially  exposed  low  dome  of  rock,  reminding  us  forcibly  of  the 
Lower  Magnesian  mounds  previously  described,  the  more  so  because  that  formation  lies 
about  two  miles  distant.  The  beds  are  exposed  on  the  east  and  south  sides,  in  which 
directions  they  dip,  but  it  is  not  certain  that  the  uncovering  of  the  other  sides  would  bear 
out  the  impression  of  a  mound  with  quaquaversal  dip,  jjiven  by  an  approach  from  the 
east  and  south.  It  may  be  here  remarked  that  the  dip  of  the  Trenton  in  this  region  is 
greater  and  more  varying  than  in  the  southern  part  of  the  state,  though  even  here  the 
inclination  rarely  exceeds  7*  or  8°.  The  rock  at  this  point  is  a  bluish  gray  argillaceous 
limestone,  with  shaly  partings  and  very  fossiliferous,  the  following  species,  many  of 
them  represented  by  a  large  number  of  individuals,  being  gathered  by  the  writer  in  a 
half  hour:  Buthotrephis  siicculens,  Spongoid  bodies  Astylospongia?  anew  species  of 
Chcetetes,  C.  discoideus,  Streptelasma  corniculum,  Schizocrinus  nodosus,  a  new  species  of 
Stictopora,  Orthis  lynx,  0.  subquadrata,  0.  testudinaria,  a  new  species  of  Orthis,  Strep- 
iorhynchus,  Strophoinena  alternata,  Leptcena  sericea,  Zygospira  recurvirostra,  a  new 
species  of  Rhynchonella,  Raphistoma  lenticularis,  an  undetermined  cast  of  Murchisonia, 
containing  a  fragment  of  Subulites,  resembling  S.  brevis,  Bellerphon  bilobatus,  Buca- 
nia  (fragment),  Orthoceras  and  Illcenus  taurus. 

In  describing  the  Lower  Magnesian  limestone  in  the  region  just  west  of  the  last  local- 
ity, its  relations  to  the  Trenton  were  dwelt  upon,  and  in  view  of  that  relationship,  it  may 
be  profitable  to  here  record  the  occurrence  of  the  following  species  in  Sees.  25  and  26, 
town  of  Ellingtou,  immediately  over  against  the  escarpment  of  Lower  Magnesian  Mine- 
stone:  Paleophycus  c&spitosum,  Schizocrinus  nodosus,  Orthis  lynx,  Streptorhynchus 
deflectum,  Strophomena  alternata,  S.  incrassata  and  an  undetermined  species  of  Khyn- 
chonella. 

By  reference  to  the  maps  it  will  be  seen  that  the  formation  passes  north  through  the 
townships'  of  Freedom,  Osborn,  Seymour,  Maple  Grove,  Lesser,  Angelica,  Little  Suam- 
ico,  Pensaukee,  Stiles,  Oconto,  Peshtigo  and  Marinette,  as  those  townships  are  now  con- 
stituted. The  exposures  in  these  towns  are  scattered  and  meager,  and  represent  chiefly 
the  lower  member  of  the  formation.  They  possess  much  local  value  as  a  source  oi 
building  material,  but  in  their  present  undeveloped  condition  they  add  but  little  of 
knowledge  or  interest  to  what  has  already  been  said,  although  they  indicate  that  the 
characteristic  peculiarities  of  the  formation  at  the  south  undergo  something  of  modi- 
fication. 

It  is  the  barrier  interposed  by  this  formation,  that  causes  the  Peshtigo  river  to  make 


304  GEOLOGY  OF  EASTERN  WISCONSIN. 

a  detour  to  the  eastward  in  range  31,  and  gives  rise  to  Potato  and  Place's  Rapids,  where 
the  river  crosses  it,  the  former  due  apparently  to  the  more  resisting  Lower  Buff  bed«  and 
the  latter  to  the  Upper. 

The  second  series  of  rapids  encountered  in  ascending  the  Menomonee  river  are  attrib- 
utable to  a  similar  cause.  It  is  much  to  be  regretted  that  at  this  extremity  of  our  dis- 
trict, two  hundred  miles  from  the  point  where  our  study  of  the  formation  began,  there  is 
not  an  equally  extensive  and  fortunate  exposure  of  its  several  members,  that  compari- 
sons might  be  made  which  would  exhibit  the  changes  it  has  undergone  in  thickness, 
lithological  character  and  organic  contents.  Instead  of  this  we  have  only  a  few  feet 
poorly  exposed  in  the  banks  of  the  Menomonee  river.  A  portion  of  the  rock  at  the 
rapids  is  a  deep  blue,  heavy,  crystalline  limestone,  weathering  smooth  and  breaking  into 
rectangular  blocks,  while  other  portions  are  quite  irregular  in  texture,  being  composed 
of  combined  earthy,  crystalline  and  shaly  material,  with  partings  of  the  latter  material. 
The  bedding  is  thin  and  the  layers  for  the  most  part  uneven.  On  the  whole,  while  not 
differing  essentially  from  the  general  characters  of  the  formation  as  seen  elsewhere,  it 
presents  an  exceptional  aspect  in  harmony  with  the  suggestion  already  made,  that  this 
formation  in  common  with  the  accompanying  ones  below  and  above  has  changed,  in  a 
subordinate  degree,  its  peculiarities.  The  following  species  indicate  the  character  of 
the  fauna:  A  new  species  of  Cruziana,  Buthotrephis  succulens,  undetermined  Fucoids, 
Chcetetes  lycoperdon,  Monticulipora  allied  to  M.  frondosa,  Crinoidea  (Cyathocrinus?), 
columns  of  Schizocrinus  nodosus,  a  new  species  of  Stictopora,  Ptilodictya  recta  ?  Orthis 
testudinaria,  O.  tricenaria,  and  an  undetermined  species,  Streptorhi/tichus  filiteoctum,  S. 
planoconvexum,  Stryphomena  incrassata,  Rhynckonella,  Zygospira  recurvirostra,  Penta- 
nierus  hemiplicatus,  and  Trilobitic  remains  (Asaphus).1 

Industrial  Considerations.  This  rock  is  extensively  quarried  for 
the  purposes  of  common  masonry.  At  the  great  majority  of  places 
the  quarries  are  only  superficial  and  the  layers  thin,  and  associated 
with  much  chipstone.  As  greater  depths  are  reached  a  better  class 
of  building  stone  is  usually  found,  because  fche  rock  has  been  less  sub- 
ject to  surface  action.  It  is  to  be  observed,  however,  that  with  the 
same  amount  of  exposure  the  layers  in  the  interior  of  a  hill,  which  ap- 
pear firm  and  solid,  would  become  split  and  broken,  like  those  that 
outcrop.  The  change  that  is  seen  in  tracing  a  layer  back  inio  the 
hill  is  brought  about  by  the  atmosphere,  frost,  percolating  water,  and 
similar  agencies,  and  is  not  due  to  the  original  nature  of  the  rock. 
This  fact  affords  a  means  of  judging  of  the  endurance  of  the  rock, 
and,  applied  to  most  of  the  beds  of  this  formation,  shows  that  their 
power  of  resisting  the  elements  is  limited.  This  is  especially  true  of 
the  Blue  limestone,  which  is  inferior  to  the  Buff,  and  which  is  to  be 
avoided  as  far  as  circumstances  will  permit.  It  is  a  matter  of  expe- 
rience that  two  quarries  may  be  opened  with  what  appears  to  the 
proprietors  an  equally  good  prospect,  one  of  which  will  soon  reach 
regular,  even  courses,  with  little  waste  material,  while  the  other  only 
develops  thin  layers  with  much  shale  and  chipstone.  Such  would  be 

1  Compare  list  from  the  same  locality  in  the  Michigan  Report,  Paleozoic  Ro.cks,  1872, 
p.  62. 


GALENA  LIMESTONE.  305 

the  case  if  one  were  located  in  the  horizon  of  the  Buff  beds,  and  the 
other  in  that  of  the  Blue.  The  facts  here  given  should  assist  in  avoid- 
ing mistakes  of  this  kind.  The  Upper  Buff  beds  furnish  the  best 
quality  of  building  stone,  unless  thick  layers  for  heavy  masonry  are 
desired,  when  the  Lower  Buff  also  furnishes  good  material.  Yery 
little  of  this  formation  is  well  adapted  for  cutting,  though  the  lower 
portions  of  the  Upper  Buff,  and  some  parts  of  the  Lower,  are  well 
suited  to  rough-dressed,  course-work,  its  soft  color,  when  tastefully 
relieved  by  appropriate  pointing,  cappings,  and  cornice,  producing  a 
very  grateful  effect.  It  is  a  significant  fact  in  this  connection,  that 
in  the  vicinity  of  Beloit,  where,  as  stated  in  the  local  descriptions, 
quarries  have  been  opened  at  nearly  every  horizon  of  this  formation, 
none  are  now  habitually  worked,  except  those  lying  in  the  lower  two- 
thirds  of  the  Upper  Buff  ~beds. 

This  limestone  is  burned  at  some  localities  for  quick  lime,  but  ex- 
cept as  a  source  of  local  supply  when  communication  is  poor,  such 
use  is  not  to  be  recommended.  The  ten  to  twenty  per  cent,  of  im- 
purities which  it  usually  contains  are  not  only  so  much  waste  mate- 
rial, as  ordinarily  manufactured,  but  if  the  heat  is  allowed  to  become 
excessive,  the  impurities  unite  with  the  lime,  producing  a  neutral 
product.  Burned  at  a  low  temperature,  this  difficulty  is  in  a  measure 
avoided.  Some  of  the  more  impure,  yet  homogeneous  portions,  would 
probably  produce  a  water  lime  that  would  fall  into  the  class  known  as 
"  limes  slightly  hydraulic,"  or  perhaps  a  grade  higher. 

GALENA  LIMESTONE. 

Reposing  on  the  Trenton  beds  just  described,  lies  the  Galena  lime- 
stone; so  named  from  the  double  fact  that  in  the  southwestern  part 
of  the  state,  where  it  has  its  most  characteristic  development,  it  is  the 
chief  formation  that  bears  the  lead  ore,  Galena  or  Galenite,  and  that  in 
the  vicinity  of  the  city  of  Galena,  it  is  extensively  displayed. 

General  characteristics.  In  chemical  constitution,  the  rock  con- 
sists essentially  of  carbonate  of  lime  and  carbonate  of  magnesia,  united, 
molecule  to  molecule,  and  hence  it  is,  strictly  speaking,  a  dolomite. 
In  addition  to  these  main  ingredients,  there  is  always  present  a  vari- 
able quantity  of  silicious  and  aluminous  material,  and  also  some 
iron.  Iron  pyrites,  calcite,  zinc  blende  and  galenite  are  not  unfre- 
quently  associated  with  it  in  the  district  under  consideration,  while 
in  the  Lead  region  these  exist  in  great  abundance,  and  others  than 
those  named  are  associated  with  them. 

The  dolomite  of  this  formation  exists  usually  in  an  imperfectly 
Wis.  SUB.— 20 


306  GEOLOGY  OF  EASTERN  WISCONSIN. 

crystallized  granular  form,  while  the  silieious  and  aluminous  mater- 
ial has  an  earthy  texture,  and  when  abundant,  gives  the  rock  a  shaly 
structure.  These  earthy  ingredients  are  usually  distributed  in  seams 
or  partings  between  the  layers,  and  in  thin  leaves  in  the  mass  of  the  bed. 
These  being  insoluble  are  left  as  a  clay  when  the  lime  and  magnesia  are 
dissolved  away,  giving  rise  to  a  clayey  soil,  or  crevice  filling  according 
to  circumstances.  When  the  rock  is  ground  up  by  glacial  action  more 
of  the  soluble  parts  are  retained  and  a  most  excellent  marly  clay  soil 
results.  In  its  more  manifest  characters  and  typical  form,  this  de- 
posit may  be  described  as  a  heavy  bedded,  irregular,  coarse  textured, 
gray  or  buff  dolomite,  containing  frequent  cavities  lined  or  filled  with 
the  minerals  already  mentioned,  and  weathering  in  a  very  irregular, 
fantastic  way,  owing  to  inequalities  of  structure.  Nodules,  and  occa- 
sionally continuous  sheets  of  chert  or  flint  are  a  prominent  feature 
of  some  portions  of  the  formation.  When  exposed  at  or  near  the 
surface,  the  rock  usually  presents  a  decayed,  rotten  appearance. 

As  a  general  description,  this  is  applicable  in  eastern  Wisconsin  as 
far  north  as  Dodge  county.  At  that  point  the  formation  begins  to 
undergo  a  change.  The  modification  consists  mainly  in  the  intro- 
duction of  more  clayey  material  in  the  form  of  shaly  leaves  and  part- 
ings. The  effect  of  this  has  been  to  render  the  rock  more  impervious 
to  water  and  atmospheric  agencies,  and  hence,  its  original  blue  or 
gray  color  is  more  generally  preserved,  and  to  this  is  added  the  green- 
ish or  bluish  hue  of  the  shaly  material,  so  that  the  rock,  instead  of 
being  light  yellowish  gray  or  buff,  is  usually  greenish  or  bluish  gray. 
W^ith  the  increase  of  argillaceous  material  there  is  also  an  increase  of 
fossils.  This  may  be  partly  due  to  the  more  perfect  preservation  that 
was  afforded  by  the  nature  of  the  rock,  but  it  is  probable  that  the 
change  in  the  oceanic  conditions  that  caused  the  increase  of  clayey 
material  also  had  its  effect  upon  the  life  of  the  period. 

Without  entering  into  a  full  discussion  of  the  causes  that  produced, 
this  modification  in  rock  and  fauna,  it  may  be  observed  that  the  ty- 
pical Galena  limestone,  viewed  as  a  whole,  arches  over  the  low  broad 
anticlinal  axis,  which  stretches  southward  from  the  more  ancieiit 
rocks  that  form  the  elevated  country  in  the  northern  part  of  the  state, 
and  that,  whatever  may  be  true  of  the  western  horn  of  this  arched 
crescent,  as  it  enters  the  trough  between  the  Wisconsin  and  Minne- 
sota axes,  the  eastern  horn  becomes  depressed  and  modified  as  it 
reaches  the  margin  of  the  great  basin  occupied  by  the  Lower  Penin- 
sula of  Michigan  and  adjacent  regions.  It  will  be  subsequently 
shown  that  there  is,  and  was  at  the  time  of  deposit,  a  marked  depres- 
sion of  all  the  formations  in  this  region,  and  that  they  were  all  mod- 


GALENA  LIMESTONE.  307 

ified  by  the  change  of  conditions  which  this  depression  caused,  aid- 
ed by  the  protection  which  the  projecting  axis  above  mentioned  and 
its  associated  reefs  aiforded.  The  change  in  the  Galena  limestone  is 
gradual  and  progressive  for  40  or  50  miles,  beyond  which  its  nature 
as  modified  becomes  constant  for  nearly  a  hundred  miles  to  the  lim- 
its of  the  state. 

Organic  Contents.  For  a  complete  list  of  the  fossils  found  in  the 
progress  of  the  survey  in  this  formation,  the  reader  is  referred  to  the 
general  table  of  fossils  of  the  Trenton,  Galena  and  Cincinnati  forma- 
tions, where  may  also  be  obtained  a  convenient  view  of  their  distribu- 
tion, and  for  a  knowledge  of  their  special  distribution  and  associa- 
tions, reference  may  be  had  to  the  lists  given  in  the  local  descriptions 
that  follow.  In  addition  to  these,  only  a  few  general  remarks  need 
here  be  made.  The  "  Lead  Coral,"  Receptaculites  Oweni,  is  the  most 
characteristic  fossil,  and,  from  the  ease  with  which  it  can  be  distin- 
guished, furnishes  a  most  convenient  and  reliable  guide.  It  is  not, 
however,  always  to  be  found  in  limited  exposures  of  the  formation, 
though  it  is  very  widely  distributed.  A  large  coiled  shell,  having  a 
high  spire,  known  as  Murchisonia  bellicincta  is  almost  equally 
characteristic  in  this  region  and  is  more  abundant.  This  species  is 
regarded  as  identical  with  Jbfurchisonid  major,  whose  typical  locality 
lies  in  this  horizon  in  the  Green  Bay  region.  Two  somewhat  similar 
fossils,  Fusispira  ventricosa  and  F.  elongata  are,  so  far  as  yet  deter- 
mined in  this  region,  confined  to  this  formation.  Lingula  quadrata, 
a  phosphatic  shell,  is  also  regarded  as  characteristic,  though  it 
is  not  strictly  confined  to  this  horizon.  Several  other  species,  so  far 
as  present  knowledge  goes,  are  found  only  in  these  beds,  but  their 
distribution  is  not  sufficiently  general  and  well  ascertained  to  justify 
regarding  them  as  distinguishing  species.  The  majority  of  the  spe- 
cies, as  we  should  expect,  are  also  -found  in  the  adjacent  formations. 
Of  the  75  species  collected  from  this  formation,  setting  aside  doubt- 
ful forms,  19  are  confined  to  it,  42  are  also  found  in  lower  strata,  but 
not  above,  and  14  are  found  both  below  and  above.  These  state- 
ments relate  only  to  the  collections  made,  and  it  is  to  be  considered 
that  owing  to  practical  difficulties,  the  collections  from  the  adjacent 
strata  above  are  less  full  than  from  those  below,  and  that  from  the 
immediately  superjacent  beds  there  are  no  collections,  because  no  ex- 
posures in  this  region. 

Thickness.  The  average  of  several  estimates  gives  this  formation 
a  thickness  of  about  160  feet,  with  a  variation  from  about  125  feet  to 
200  feet. 

Industrial  value.     While  this  is  the  formation  which  is  so  pro- 


308  GEOLOGY  OF  EASTERN  WISCONSIN. 

ductive  of  lead  arid  zinc  in  the  southwestern  part  of  the  state,  there 
is  little  reason  to  expect  that  it  will  prove  so  in  the  region  under  con- 
sideration, for,  although  the  ores  of  those  metals  occur  not  unfre- 
quently  in  small  quantities,  no  indications  of  valuable  deposits  have 
yet  been  developed. 

Analysis  shows  that  much  of  this  formation  from  Dodge  county 
southward  is  a  comparatively  pure  magnesian  limestone,  and  is  well 
adapted  to  the  manufacture  of  quicklime.  It  is  used  for  this  pur- 
pose at  Watertown,  Ft.  Atkinson,  Whitewater  and  elsewhere.  It  is 
estimated  that  40,000  to  50,000  barrels  are  burned  annually.  It  is 
much  to  be  preferred  to  the  Trenton  beds  which  are  sometimes 
burned  in  the  inlmediate  vicinity. 

In  the  southern  portion  of  the  district  it  furnishes  an  inferior 
building  stone,  owing  to  its  granular  character,  but  as  it  undergoes 
modification  farther  north,  it  becomes  better  suited  to  the  purposes 
of  construction.  At  "Waupun,  Oshkosh  and  other  localities,  it  is 
rough-dressed  for  course-work  with  very  satisfactory  results.  At 
other  points,  especially  Duck  Creek  and  Kaukauna,  the  heavy  beds 
are  well  suited  to  the  more  massive  kinds  of  masonry,  and  have  been 
used  in  the  construction  of  the  government  works  in  that  region. 

Distribution  and  Local  Details.  The  more  exact  surface  distribu- 
tion of  the  Galena  limestone  is  shown  on  the  maps  of  the  accompa- 
nying atlas.  Viewed  in  a  comprehensive  way  the  formation  may  be 
said  to  constitute  a  broad,  nearly  north  and  south  belt,  having  a  jag- 
ged, irregular  outline,  and  forming  the  floor  of  the  great  Rock  river 
and  Green  Bay  valley. 

Beginning  at  the  south,  according  to  our  habit,  we  find  on  the  west  side  of  Rock  river, 
in  Rock  county,  about  a  dozen  small  areas  of  this  formation,  capping  the  higher  prom- 
inences. Only  a  few  feet  of  the  base  of  the  formation  are  present  at  these  points. 

In  the  eastern  part  of  Rock  county,  and  the  western  part  of  Walworth  county,  the 
Galena  limestone  has  a  more  ample  development,  though  largely  concealed  by  drift.  The 
rock  in  this  region  has  essentially  the  same  characteristics  that  distinguish  it  in  the  Lead 
region,  being  a  rather  heavy  bedded,  coarse,  uneven  textured,  granular,  buff  dolomite, 
containing  more  or  less  of  chert,  and  weathering  to  a  very  rough  exterior.  Fossils  are 
not  abundant,  and  are  usually  in  the  condition  of  obscure  casts.  The  most  extensive 
exposures  are  found  where  the  westward  flowing  streams  have  formed  gorges  in  crossing 
the  strata. 

The  Western  Union  Railway  passes  through  one  of  these,  in  the  town  of  Turtle, 
about  midway  between  Beloit  and  Clinton  Junction,  and  has  added  several  fine  cuts  to 
the  natural  exposures  made  by  the  stream. 

In  the  town  of  Bradford,  the  Turtle  creek  has  excavated  a  passage  through  this  for- 
mation, leaving  vertical  escarpments  of  moderate  altitude,  surmounted  by  steep  slopes, 
rising  from  80  feet  to  100  feet  above  the  stream.  Fissures  analogous  to  those  of  the 
Lead  region  occur  here,  but  no  trustworthy  indication  of  valuable  lead  deposits  were 
seen.  A  few  fossils  were  collected  here,  including  Receptaculites  Otceni,  an  undeter- 


GALENA  LIMESTONE.  309 

mined  species  of  Streptelconta,  a  new  species  of  Lingula,  Oiihis  lynx,  0  tricenaria.  a 
Strop Jiomena,  Cypricardites  rotundatus,  C.  subtruncatus,  C.  ventricosus,  Raphistoma  len- 
ticitlaris,  Trochonema  umbiUcatum,  a  new  species  of  Murchisonia  and  Orthoceras  junce- 
i(»t.  The  most  southerly  exposure  of  this  formation,  seen  in  Walworth  county,  was  near 
Sharon  Mills.  Between  this  point  and  Whitewater,  deep  drift  conceals  it.  Near 
the  latter  point,  several  quarries  have  been  opened,  from  which  a  supply  of  building 
stone  and  lime  are  derived.  The  rock  here  is  of  a  more  decided  buff  color  than  is  com- 
mon, and  is  marked  with  peculiar  concentric  wavy  lines  of  a  redish  hue.  It  is  soft,  po- 
rous, granular,  uneven  in  texture,  and  much  decomposed  on  the  surface,  but  is  more 
cohesive  and  enduring  than  its  appearance  would  indicate.  There  is  evidence  of  a  con- 
siderable fauna  at  this  point,  though  the  preservation  of  the  fossils  is  usually  poor. 

The  following  identifications  have  been  made,  a  portion  of  them  based  on  specimena 
from  the  private  collections  of  Mr.  L.  C.  Wooster: 

Receptaculites  globosus,  R.  Oweni,  Astylospongia,  casts  of  the  cup  of  a  Zaphrentis, 
Cornulites-like  tubes,  Lingula  quadrata,  a  Monomerella,  Orthis  lynx,  0.  perveta,  or  equi- 
rahis,  Streptorhynchus  deltoideum,  Strophomena  alternate,  S.  camerata,  large  form,  S. 
camerata?,  small  ventricose  form,  Atrypa  bisulcata,  Rhtjnchonella  capax,  Anibonych'm 
erecta?,  A.  lamellosa,  Cypricardites  ventricosus,  Raphistoma  lenticularis,  Trochonema 
umbilicatum,  Pleitrotomaria,  resembling  P.  Occidentalis,  Murchisonia  bellicincta,  or  M. 
major;  M.  bicincta,  and  anew  species,  Holopea  paludiniformis,  H.  near  H.  obliqua, 
Fusispira  elongat-t,  F.  ventricosa,  and  a  new  species  of  Ecculiomphalus,  Maclurea 
Bigsbyi?,  and  two  n.  sp.  Conularia  Trentonensis,  Orthoceras  planoconvexum,  and  two 
undetermined  species,  Cyrtoceras  (Oncoceras)  plebeium,  and  two  undetermined  species. 

Passing  by  several  minor  exposures,  we  find  about  two  miles  southeast  of  Fort 
Atkinson,  quarries  situated  in  the  lower  portion  of  this  formation,  and  a  little  to  the 
north  (Sec.  10,  S.  E.  qr.,  T.  5,  R.  14),  a  quarry  in  the  Upper  Blue  limestone.  The  rock 
from  the  former  furnishes  a  good  lime  and  an  ordinary  building  stone.  On  the  west 
side  of  Rock  river,  in  the  towns  of  Jefferson  and  Oakland,  are  several  patches  of 
Galena  limestone,  forming  the  nucleus  of  the  prominent  hills  of  that  region.  On  the 
east  side  of  the  river,  the  heavy  drift  accumulations  effectually  conceal  the  formation. 

About  two  miles  north  of  Watertown,  in  the  S.  E.  qr.  of  Sec.  20,  town  of  Emmet, 
Dodge  county,  is  an  extensive  quarry  displaying  this  formation,  which  still  maintains 
the  characteristics  already  described.  Cavities  in  the  rock  are  rather  more  than  usually 
abundant,  and  are  usually  lined  with  calcite,  or  more  rarely  dolomite,  and  occasionally 
with  zinc  blende  or  galena.  Iron  pyrites  also  occur  in  nodular  crystallizations,  many 
of  which  are  desulphurized  in  whole  or  in  part. 

Chert,  as  usual,  is  abundant,  more  particularly  in  the  upper  layers.     Fossils  are  rare. 

An  analysis  by  Mr.  Bode  of  chippings  from  the  several  layers  representing  a  thick- 
ness of  fifteen  feet,  shows  the  following  composition: 

Carbonate  of  lime 54.051 

Carbonate  of  magnesia 44. 139 

Silica 1 . 564 

Alumina 0.072 

Oxide  of  iron 0 . 174 


100.000 

From  which  it  will  be  seen  to  be  a  nearly  pure  dolomite,  aside  from  the  chert,  which 
was  excluded  from  the  specimens  analyzed. 

As  far  north  as  this  point,  the  rock  of  this  formation  has  maintained  a  very  constant 
character,  and,  as  remarked  before,  closely  resembles  the  Galena  in  its  more  typical 
localities.  To  the  north  of  this  point  it  begins  to  undergo  a  change.  For  twenty-five 


310  GEOLOGY  OF  EASTERN  WISCONSIN. 

miles  northward  the  change  is  slight.  The  rock  becomes  somewhat  more  firm,  compact, 
and  serviceable  as  building  material  and  of  a  gray  or  blue  cast  rather  than  buff.  It  is 
also  somewhat  more  argillaceous. 

In  the  vicinity  of  Fox  Lake  and  at  Waupun,  this  change  has  become  quite  pro- 
nounced, resulting  in  a  rock,  much  superior  to  that  farther  south,  for  purposes  of  con- 
struction, though  less  serviceable  for  quicklime.  If  the  formation  be  traced  along  its 
western  margin,  that  is,  along  its  base,  the  modification  of  its  characteristics  is  found  to 
be  very  gradual.  Along  the  upper  margin,  there  are  but  few  opportunities  for  ex- 
amination. 

At  Seven  Mile  Creek  there  is  a  flat  weathered  exposure  that  reveals  little,  save  the 
fact  of  change  in  the  direction  indicated.  Moore's  quarry  in  the  western  part  of  the  city 
of  Fond  du  Lac  displays  a  rough,  coarse,  thick  bedded  rock  of  irregular  texture,  con- 
taming  cavities  lined  with  calcite  and  pyrite,  and  somewhat,  though  not  remarkably,  ar- 
gillaceous. While  different  from  the  rock  at  Watertown  and  southward,  it  still  retains 
a  noticeable  resemblance  to  it.  Beceptaculites  Oweni  and  Murchisonia  bellicincta  (major) 
occur  here,  as  well  as  at  Waupun  and  other  points  in  this  region,  and  leave  no  doubt  as 
to  the  horizon  to  which  these  beds  belong.  At  Moore's  quarry  the  strata  have  been 
forced  up  into  a  sharp  anticlinal  axis,  from  which  the  beds  dip  equally  in  both  directions 
at  an  inclination  of  upwards  of  10.°  The  trend  of  the  axis  is  northwest  and  southeast. 
It  is  manifestly  a  case  of  disturbed  strata,  but  the  extent  of  the  distubance  is  unknown, 
as  the  excavation  is  very  limited.  It  is  interesting  chiefly  because  such  features  are 
very  rare  in  this  quiet  region.  While  sloping  and  undulating  beds  are  not  at  all  un- 
common, they  almost  invariably  carry  with  them  evidences  that  they  were  so  deposited 
rather  than  folded  or  tilted  by  subsequent  force. 

Beyond  this  point,  so  far  as  known  to  me,  the  Galena  formation  has  not  been  mapped 
by  previous  investigators,  and  most,  if  not  all  of  the  rocks  north  of  this  point,  now  re- 
ferred to  that  horizon,  have  heretofore  been  placed  either  in  the  Trenton  series  below,  or 
the  Cincinnati  above,  and  lest  the  position  now  taken  should  be  misapprehended,  it 
must  be  borne  in  mind,  that  it  is  simply  claimed  that  the  beds  in  question  belong  to  the 
Galena  horizon,  and  are  a  continuation  of  the  unquestioned  strata  of  that  formation  as 
found  to  the  southward,  and  since  they  are  the  exact  stratigraphical  equivalents  of  the 
lead-bearing  beds,  they  are  mapped  and  described  as  being  a  modified  form,  of  that  sub- 
division of  the  Trenton  group.  Whether  the  term  Galena  limestone  should  be  applied 
to  this  group  of  strata  as  far  as  they  are  directly  traceable,  or  whether  it  should  be  lim- 
ited to  the  lead-bearing  portion,  or  whether  it  should  apply  to  that  portion  which  has 
the  same  lithological  character  as  the  lead-bearing  portion,  but  is  not  itself  productive, 
as  for  instance,  that  portion  now  described,  or  whether  it  should  be  extended  as  far  as  a 
similarity  of  organic  remains  is  found,  which  would  include  a  portion  whose  lithoiogical 
characters  differ  from  the  typical  Galena  limestone,  is  not  here  discussed,  and  is  a  mat- 
ter of  little  practical  importance,  except  as  a  means  to  a  clear  understanding  of  the  facts. 

But  it  is  a  matter  of  much  importance  to  ascertain  precisely  what  becomes  of  the  lead- 
bearing  formation  as  it  recedes  from  the  productive  area  in  southwestern  Wisconsin, 
since  it  adds  to  our  knowledge  of  the  conditions  under  which  the  formation  had  its 
origin,  and  which,  it  is  commonly  held,  determined  its  metalliferous  character.  About 
two  miles  southwest  of  Oshkosh  are  quarries  that  possess  unusual  interest,  on  account 
of  their  relation  to  this  qiiestiou.  Two  kinds  of  rock  are  displayed  by  the  excavations. 
The  lower  portion,  consisting  of  an  exposure  of  15%  feet,  is  formed  of  regular,  uniform 
layers  from  4  to  10  inches  in  thickness,  rarely  more  or  less,  of  a  crystalline,  compact, 
hard,  brittle,  subtranslucent,  magnesian  limestone,  marked  at  intervals  with  irregular 
argillaceous  seams  of  a  deep  blue  color,  occasionally  tinged  with  green.  These  shaly 
partings  are  usually  clustered  about  the  bedding  joints,  to  which  they  probably  stand  in 
the  relation  of  cause.  Aside  from  these  seams,  the  mass  of  the  rock  is  a  dark  bluish 


GALENA  LIMESTONE.  311 

gray.  The  specific  gravity  is  high.  Geodes  are  common,  and  are  usually  filled  with  cal- 
cite  in  a  great  variety  of  forms  of  crystallization,  and  with  pyrite,  also  in  unusual  variety 
of  forms  and  colors.  Zinc  blende  is  also  quite  common,  and  more  rarely,  Galena.  This 
combination  often  gives  to  these  geodes  a  very  beautiful  and  interesting  appearance. 
Sheets  of  iron  pyrites,  filling  vertical  fissures,  sometimes  traverse  the  quarries.  Zinc 
blende  is  sometimes  found  in  small  lumps  in  the  interior  of  the  beds.  Fossils  are  some- 
what rare  in  this  portion,  Receptaculites  Oweni  being  most  frequent.  Columns  of  Schiz- 
ocrinus,  and  a  fragment  of  an  Endoceras  were  also  found  by  diligent  search. 

The  upper  portion  of  the  quarry  consists  of  alternating  beds  of  limestone  and  shale, 
the  whole  having  a  greenish  gray  color.  The  limestone  is  much  more  impure  and  less 
crystalline  than  that  below,  and  of  a  less  firm  character.  These  beds,  and  more  especi- 
ally the  associated  shales,  are  quite  fossiliferous.  Among  the  species  represented  are 
the  following: 

Small  spherical  bodies  (sponges?),  Chcetetes  lycoperdon,  C.  discoideus,  a  new  species 
of  C.  (branching  form),  Zaphrentis  (res.  Streptelasma  multilamellosum),  Schizocrinus 
nodosus?  (large  size  column),  Homocrinus,  a  new  species  of  Stictopom,  a  new  species  of 
Trematoporn,  a  new  species  of  Lingula,  Crania  scabiosa  on  Streptelasma,  Orthis  lynx, 
0.  plicatella?  0.  testudinaria,  0.  tricenaria,  Streptorhynchus  deltoideum,  Sfrophomcna 
alternate/,,  S.  camerata,  S.  incrassata,  Leptcena  sericea,  Zygospira  recuvirostris,  a  new 
species  of  Rhynchonella,  Ambonychia  radiata?  Cypricardites  (internal  cast),  Tellinomya 
(internal  cast)  Euomphalus,  Murchisonia  bellicincta  =  M.  Major,  Bellerophon  biloba- 
tus,  Illcenus  taurus  (pygidium),  Calymene  senaria,  Harpes?  (fragment  of  cheek  spine), 
Ceraurus  pleurexanthemus. 

A  specimen  of  Receptaculites  Oweni  was  found  in  the  rock  pile,  adjacent  to  the  quar- 
ries, and  was  believed  to  have  come  from  the  upper  layers. 

It  will  be  best  to  reserve  a  discussion  of  the  interesting  facts  here  presented  until  the 
data  furnished  farther  north  are  before  us,  and  while  noting  on  the  map  the  position 
and  stratigraphical  relations  of  these  quarries,  pass  on  along  the  strike  of  the  formation 
to  the  vicinity  of  Neenah. 

About  a  mile  southeast  of  this  place,  the  rock  comes  to  the  surface  and  is  quar- 
ried to  the  depth  of  a  few  feet.  Like  the  upper  portion  of  the  quarries  at  Oshkosh, 
there  is  an  alternation  of  impure  limestone  and  shale.  There  is  also  present  a  coarse, 
granular  crystalline  rock  of  firmer  texture  than  the  remaining  layers.  The  dip  is  irreg- 
ular, varying  from  8°  downwards.  Some  layers,  especially  the  shaly  ones,  are  quite  fos- 
siliferous. The  following  species  occur  here: 

ButhotrejMs  succulens,  Graptolites,  Choetetes  lycoperdon,  and  a  new  species  having 
a  branching  form,  discs  of  Schizocrinus,  plates  of  Crinoids,  two  new  species  of  Tre- 
matopora,  two  new  species  of  Stictopora,  a  Ptilodictya,  Lingula  quadrata,  Orthis  lynx, 
0.  pectinella,  0.  testudinaria,  and  a  new  species,  Hemipronites  Americanus,  Strepto- 
rhynchus  deltoideum,  Leptcena  sericea  (small  one)  Zygospira  modesta;  a  new  species  of 
Rhynchonella,  an  undetermined  species  of  Ambonychia,  and  of  Euomphalus,  Raphis- 
toma  lenticularis  (small),  Helicotoma  planulata,  Murchisonia  bellicincta,  M.  Gracilis, 
Conularia  Trentonensis,  an  Orthoceras,  a  Cyrtoceras,  Leperditia  fabulites,  Ill&nus 
lowensis,  I.  taurus,  Calymene  senaria  and  Dalmania  callicephalas. 

The  facies  of  this  fauna,  as  well  as  the  nature  of  the  beds,  show  a  somewhat  wide 
departure  from  the  character  of  the  typical  Galena  limestone,  and  a  close  alliance  with 
the  Upper  Blue  beds  of  the  Trenton;  but  the  facts  yet  to  be  given  will,  it  is  believed, 
justify  the  position  to  which  they  are  assigned. 

Three  miles  north  of  this,  in  the  town  of  Menasha  (Sec.  11,  E  hf .  of  S.  W.  qr.),  are  two 
quarries  only  a  short  distance  apart,  but  owing  to  the  irregular  nature  of  the  dip,  it  is 
not  clear  precisely  what  relation  they  sustain  to  each  other.  The  quarry  south  of  Mr. 
Hunt's  house  consists  of  impure  argillaceous  greenish  blue  limestone,  alternating  with 


312  GEOLOGY  OF  EASTERN  WISCONSIN. 

shaly  layers  and  partings,  closely  resembling  the  upper  beds  at  the  Oshkosh  quarries, 
and  carrying  about  the  same  fossils. 

The  more  recently  opened  quarry  north  of  this,  so  far  as  developed  at  the  time  of  my 
visit,  showed  a  more  granular  rock,  abounding  in  chert.  It  is  important  to  note  that 
here,  Beceptaculites  Oweni,  B.  lowensis  and  Murchisonia  bellicincta,  fossils  that  charac- 
terize the  Galena  horizon,  occur,  associated  with  Choetetes  lycoperdon,  a  new  species  of 
Chvetetes  having  a  large  branching  form,  Streptelasrna  corniculum,  Schizocrhnts  nodo- 
sus,  a  new  species  of  Stictopora,  Orthis  lynx,  0.  testudinaria,  0.  disparaUs,  0.  pectinella, 
0.  tricenaria,  ittrophotnena  incrassata,  Leptcena  sericea,  a  new  species  .of  Rhynchonella, 
Baphistoma  lenticularis,  a  Helicotoma,  resembUng  H.  planulata,  two  species  resembling 
Murchisonia  bellicincta,  one  resembling  M.  gracilis,  and  one  Uke  M.  percarinata;  a  Belle- 
rophon,  a  doubtful  form  of  Holopea  paludiniformis,  and  an  undetermined  Orthoceras. 
From  Appleton  to  De  Pere,  the  Lower  Fox  river  forms  a  succession  of  rapids  over 
the  heavier  and  more  resisting  ledges  of  this  formation.  A  description  of  the  beds  at 
Kaukauna  will  sufficiently  indicate  the  general  character  of  the  whole.  At  that  point 
the  layers  vary  from  6  to  30  inches  in  thickness,  and  have  a  dip  of  from  1%C  to  2°  to  the 
S.  of  E.  The  rock  is  of  a  dull  bluish  green  or  gray  hue,  and  is  characterized  by  very  thin, 
shaly  partings  between  some  of  the  layers,  and  by  thin,  irregular,  argillaceous  laminae 
through  the  body  of  the  rock,  not  sufficient  however  to  notably  impair  its  strength  or 
powers  of  resisting  atmospheric  influences,  since  bowlders,  that  have  apparently  been  ex- 
posed since  the  drift  period,  are  still  sound.  Aside  from  these  laminse,  the  rock  has  a 
crystalline  character,  impervious,  and  compact  in  general,  though  it  contains  a  few  cav- 
ities, some  of  which  are  lined  with  calcite,  and  occasionally,  pyrite.  The  beds  are  ver- 
tically fissured  at  intervals,  affording  facilities  for  easy  quarrying.  Some  of  these  fissures 
are  lined  with  calcite  or  pyrite. 

These  layers  contain  comparatively  few  fossils.  The  most  conspicuous  and  character- 
istic are  Marchisonia  bellicincta  (major),  Lingula  quadrata,  and  Fusispira  ventricosa. 
With  these  are  associated  several  other  species,  already  mentioned  as  occurring  at  Osh- 
kosh, Neenah  and  Menasha.  At  Little  Chute,  a  Climacograptus,  nearly  allied  to  C.  typ- 
icalis,  occurs,  and  also  north  of  this,  in  equivalent  strata  on  Duck  creek,  but  is  not  known 
to  be  found  at  any  other  horizon.  An  analysis  shows  this  rock  to  be  a  dolomite,  with 
about  8  per  cent  of  impurities,  consisting  chiefly  of  silica,  alumina  and  iron. 

Duck  creek,  which  runs  nearly  parallel  to  the  Fox  river,  has  also  cut  away  the  drift 
and  displayed  this  formation.  At  the  village  of  Duck  Creek,  near  its  mouth,  the  mas- 
sive beds  are  strikingly  similar  to  those  at  Kaukauna,  both  in  lithological  characters 
and  in  organic  contents.  Murchisonia  bellicincta,  Fusispira  ventricosa  and  Lingula, 
quadrata  are  again  the  most  noteworthy  fossils.  Farther  up  the  stream,  the  beds  sire 
more  argillaceous  and  alternate  with  shaly,  very  fossiliferous  layers,  closely  resembling 
those  already  described.  The  leading  fossils  are  graptolitic  remains.  Chcetetes  ly coper- 
don  and  a  large  new  species  of  the  same  genus,  Streptelasma  corniculum,  Pleurocystitcs, 
Glyptocystites  Logani,  a  Trematopora,  Lingula  quadrata,  and  a  species  resembling  L. 
attenuata,  Orthis  pectinella,  and  a  new  species,  Strophomena  alternata,  S.  incrassata  ? 
Rhynclwnella  capax,  Baphistoma  lenticularis,  Trochonema  umbilicatum,  Murchisonia 
bellicincta  and  Dalmania  callicephala. 

Duck  creek,  as  well  as  the  Fox  river,  runs  along  the  line  of  drift  movement,  but  in  the 
opposite  direction.  The  glacier  moved  up  these  valleys  and  planed,  polished  and 
grooved  the  surface  of  the  rock  in  the  most  beautiful  manner,  as  may  be  observed  at 
any  favorable  locality.  In  this  planing  process,  the  softer  portions  of  the  rock  were 
doubtless  excavated  deepest,  leaving  the  more  resisting  portions  prominent,  and  these 
portions  form  the  rapids  on  these  streams,  and  are  the  parts  chiefly  observed.  The 
more  shaly  portions  are  not  observed  at  all  on  the  Fox  river,  and  at  but  few  localities 
on  Duck  Creek. 


GALENA  LIMESTONE.  313 

The  Big  Suamico  river  has  likewise  denuded  this  formation  at  a  few  points.  The  most 
noteworthy  of  these  is  at  Flintville,  and  as  the  section  here  best  illustrates  the  peculi- 
arities which  the  formation  has  assumed,  it  may  be  described  in  some  detail. 

1.  The  lowest  rock  seen  is  a  bed  of  soft,  bluish-green,  disintegrating  shale,  only  par- 
tially exposed. 

2.  Above  this,  is  a  three-inch  layer  of  coarse,  blue,  granular,  half  crystalline  limestone, 
mixed  with  earthy,  argillaceous  material,  and  at  all  points  very  full  of  Orthis  testud'maria. 

3.  Upon  this,  rest  10  inches  of  soft,  bluish-green,  decomposed  shale,  containing  nurn- 
ulitic  forms  of  Chcetetes  and  Streptelasma  corniculum. 

4.  Above  this,  lies  a  four- inch  bed  of  d«ep  blue,  coarse-grained,  crystalline  magnesian 
limestone,  mixed  with  more  or  less  of  yellowish,  earthy  matter,  the  whole  having  a  high 
specific  gravity.    This  layer  is  characterized  by  the  presence  in  unusual  numbers  of 
Receptaculites  Oweni,  the  characteristic  fossil  of  the  Galena  limestone,  while  other  fossils, 
except  minute  crinoidal  discs,  are  rare. 

5.  Upon  this,  repose  2  feet  10  inches  of  shale  and  impure  limestone,  easily  decompos- 
ing on  exposure,  and  containing  many  branching  forms  of  Chcetetes,  Streptelasma  cor- 
niculum, Orthifi  lynx,  0.j)licatellaiLeptcena  sericea,  and  other  fossils. 

6.  Next  above,  occurs  a  10  inch  layer,  similar  to  No.  4,  but  more  massive,  and  marked 
by  irregular  laminae  of  a  dark,  dirty  greenish,  argillaceous,  and  apparently  carbonaceous 
material,  giving  a  somewhat  fetid  odor  under  the  stroke  of  the  hammer. 

7.  Five  inches  soft  shale,  similar  to  No.  3. 

8.  A  four-inch  layer,  similar  to  No.  5,  but  more  markedly  blue. 

9.  An  irregular  layer,  about  2  inches  thick,  that  is  little  else  than  a  mass  of  the  stems 
of  the  branching  Chcetetes.    The  numulitic  forms,  as  also  Brachiopoih  and  Trilobites,  are 
present. 

10.  About  1  foot  6  inches  of  shale,  containing  Chcetetes  in  abundance,  especially  the 
more  hemispherical  forms. 

11.  Above  this,  lie  about  3  feet  of  thick  bedded,  massive  dolomite,  very  similar  to  that 
previously  described  at  Kaukauna  and  Duck  Creek.     It  contains  Receptaculites  Oweni, 
besides  Orthis  plicatella,  0.  lynx,  Leptcena  sericea,  Strophomena  alternata,  Raphistonict 
lenticularis,  and  fragments  of  trilobites  and  crinoids. 

The  entire  collection  made  at  this  locality,  which  is  given  below,  shows  an  interesting 
mingling  of  those  species  that  are  characteristic  of  the  Galena  limestone  in  its  typical 
localities,  with  an  abundant  Trenton  fauna  not  found  at  this  horizon  in  the  Lead  region. 
Cruziana  ?  Receptaculites  Oweni,  Chcetetes  lycoperdon,  and  three  new  species,  Strepte- 
lasma corniculum,  two  new  species  of  Stictopora,  Lingula  attenuata  ?  Philodops  truncata, 
Orthis  lynx,  0.  plicatella,  and  a  form  with  bifurcating  ribs  like  0.  fissicosta,  0.  testudl- 
naria,  Hemipronites  Americanus,  n.  sp.,  Strophomena  alternata,  S.  incrassata  ?  Lep- 
tcena sericea,  Zygospira  recurvirostris,  a  new  species  of  Rhynchonella,  Pentamerus 
(Camerdla?)  hemiplicatus,  Raphistoma  lenticularis,  Murchisonia  bellicincta  (slender 
form),  Murchisonia  (slender  form  like  M.  gracilis,  round  volutions),  Fusispira  elongata, 
Bellerop}ion  bilobatus,  Cyrtolites  Di/eri,  Endoceras  proteiforme,  Illcenus  taurus,  I. 
loivensis,  Asaphus,  Calymene  senaria,  Ceraurus  pleurexanthemus,  Dalmania  calli- 
cephala,  Spherocori/phe,  sp.?  andProetus?  (fragment  only). 

Tin's  formation,  without  noteworthy  modification,  is  again  exposed  by  the  Little  Sua- 
mico river,  and  outcrops  along  the  shore  of  Green  Bay,  south  of  Pensaukee,  and,  al- 
though largely  concealed  by  drift,  borders  the  bay  northward  into  Michigan. 

Its  last  appearance  in  the  state  is  at  the  lower  rapids  of  the  Menomonee  river,  a  little 
above  Marinette,  where  a  few  feet  are  expised  in  the  channel  of  the  river.  It  is  here 
a  bluish  or  greenish  gray,  impure  dolomite  of  rather  coarse,  uneven,  partly  crystalline 
and  partly  earthy  texture,  containing  some  cavities  lined  with  calcite.  Fossils  are  not 
abundant.  Dr.  Rominger,  in  the  Michigan  report,  cites  the  following:  "Lingula 


314:  GEOLOGY  OF  EASTERN  WISCONSIN. 

quadrata,  Leptsena  canierata,  Streptorhynchus  filitextus,  Murchisonia  major,  Bucania 
expansa,  Trochonema  umbilicata,  Maclurea  (large  casts,  three  inches  in  diameter),  Con- 
ularia  Trentonensis,  Dictyonema  (a  species  with  veiy  delicately  reticulated  fronds  ex- 
panding from  a  transversely-wrinkled  hollow  cylindrical  stem,  with  a  shining  carbon- 
aceous surface) ;  also  indistinct  specimens  of  Chsetetes  frondosus  and  Crinoid  stems  are 
included  in  the  rock,"  p.  57;  to  which  may  be  added  a  new  species  of  Stictopora,  Ra- 
phistorna  lenticularis,  a  Murchisonia  allied  to  M.  gracilis,  but  larger,  a  Pleurotomaria, 
and  an  Orthoceras. 

In  the  way  of  recapitulation,  it  may  be  observed  that  a  comparison 
of  the  fossils  that  have  now  been  enumerated,  in  connection  with  the 
several  localities,  shows,  (1)  that  there  are  a  considerable  number  that 
range  throughout  the  whole  Trenton  period,  including  the  Cincinnati 
epoch,  and  are,  therefore,  of  no  service  in  discriminating  between  its 
subdivisions;  (2)  that  there  is  another  portion  whose  occurrence  is 
chiefly  confined  to  the  strata  below;  and  (3)  that  there  are  a  few  that 
are  not  authentically  known  to  occur  either  above,  or  below,  the  horizon 
under  consideration,  and  may  be  regarded  as  characteristic  of  it.  Of 
this  latter  number,  Receptaculites  Oweni  and  Murchisonia  bellicincta, 
or  major,  are  the  most  constant  and  reliable.  Lingula  quadrata,  al- 
though rare  in  other  beds  in  this  region,  does  not  appear  to  be  strictly 
confined  to  this  subdivision.  Fusispira  ventricosa,  F.  elongata,  and 
an  intermediate  form,  are,  perhaps,  to  be  added  to  the  list,  as  they  range 
from  Walworth  to  Oconto  county,  and  are  not  found  in  the  collec- 
tions of  the  survey  in  any  other  stratum. 

It  will  be  seen  that  the  change  in  the  nature  of  the  rock  com- 
menced in  Dodge  county,  and  was  essentially  completed  in  Winnebago 
county,  being  gradual  and  progressive  through  -iO  or  50  miles;  and 
that  it  consisted  mainly  of  the  addition  of  shaly  or  argillaceous  mate- 
rial; and  that  the  increase  in  the  variety  and  number  of  the  fossils  ac- 
companied the  increase  of  the  clayey  ingredient. 

By  a  comparison  with  the  formations  already  described,  and  those 
remaining  to  be  treated,  it  will  further  be  seen,  that  they  also  undergo 
some  modification  at  essentially  the  same  latitude,  the  cause  of  which 
can  be  better  understood  when  all  the  facts  are  before  us. 


THE  CINCINNATI  SHALES  AND  LIMESTONES. 

The  Galena  limestone  is  succeeded  by  a  series  of  shales  and  lime- 
stones, constituting  what  will  be  known  in  this  report  as  the  Cincin- 
nati group,  a  name  now  quite  generally  adopted  for  this  geological 
horizon,  although  there  is  still  some  difference  of  opinion  as  to  the 
lower  limits  which  should  be  assigned  to  the  application  of  the  term. 
It  here  includes  all  the  beds  known  to  lie  between  the  upper  surface 


THE  CINCINNATI  SHALES  AND  LIMESTONE.  315 

of  the  Galena  limestone,  and  the  upper  limits  of  the  Lower  Silurian 
formation. 

General  Character.  The  shales  that  form  so  prominent  a  member 
of  this  group  are  of  a  varied  character.  One  kind  is  little  else  than  a 
slightly  indurated  green  or  blue  clay,  often  very  fine  in  texture,  con- 
taining but  little  sand,  or  other  hard  material,  and  being,  chemically, 
little  else  than  silicate  of  alumina.  This  graduates,  by  the  addition  of 
fossils,  iron  pyrites,  calcareous  and  silicious  matter,  and,  occasionally, 
crystals  of  gypsum,  into  a  variety  of  impure  and  changeable  shales. 
Another  class  has  :i  more  slaty  structure,  having  been  deposited  in 
delicate  laminse  of  fine  sediment,  not  so  largely  clay  as  the  above. 
These  split  with  great  ease  arid  regularity  into  thin,  brittle  plates. 
Still  another  kind  lias  a  more  arenaceous  character  and  regular  bed- 
ding, giving  it  somewhat  the  appearance  of  a  fine  grained  sandstone. 
These  three  general  classes  include  many  minor  varieties. 

The  associated  limestone  is  also  varying  in  nature.  A  portion  has 
a  coarse,  granular,  crystalline  texture,  mingled  with  earthy,  or  ocher- 
ous  matter,  while  another  portion  is  compact,  crystalline,  with  leaves 
of  argillaceous  matter  variously  distributed  through  it;  and  still  other 
portions  are  silicious  or  cherty.  These  several  forms  often  give  place 
to,  or  graduate  into  shale.  The  limestone  occurs  at  all  observed  hori- 
zons, but,  except  at  the  northern  extremity  of  the  exposure,  is  much 
less  in  quantity  than  the  shale.  Near  Little  Sturgeon  Bay,  the  cal- 
careous material  is  much  increased,  and  limestone  predominates. 

The  upper  part  of  the  formation  is  chiefly  composed  of  the  clay- 
shales  and  limestone. 

The  slaty  and  arenaceous  shales  are  found  at  lower  horizons.  Their 
special  positions  and  distribution  may  be  found  among  the  local  de- 
tails. 

The  thickness  of  the  formation  may  be  placed  at  200  feet,  with  an 
ascertained  variation  from  165  feet  to  240  feet.  There  are  reasons  for 
believing  that  the  extreme  range  is  somewhat  greater. 

Life.  Sea  weeds  represented  the  plants,  and  Radiates,  Mollusks, 
and  Articulates,  the  animals. 

The  most  noteworthy  feature  is  the  remarkable  abundance  of  Chsete- 
toid  Corals  and  Bryozoans  at  certain  localities.  Upwards  of  30  species 
were  collected  from  the  shale  thrown  out  of  two  shafts  of  no  consid- 
erable depth.  Other  Corals,  than  those  related  to  Chaetetes,  are  far  less 
abundant.  Brachiopods  are  next  in  prevalence,  the  genera  Orthis  and 
Strophomena  predominating.  Lamellibranchs  and  Gasteropods  are 
rare,  and  Crustaceans  and  Crinoids  limited  to  a  few  species.  More 
specific  facts  will  be  given  with  the  local  details,  and  a  full  list,  ex- 


316  GEOLOGY  OF  EASTERN  WKOON8IN. 

cept  some  new  or  doubtful  species,  may  be  found  in  the  table  of  fossils 
of  the  Trenton  period. 

Industrial  value.  This  formation  makes  two  notable  contributions 
to  the  soil  derived  from  it,  either  directly,  or  through  the  medium  of 
the  drift.  The  one  arises  from  the  clayey  members  of  the  formation, 
and  furnishes  an  argillaceous  constituent  to  the  soil.  They  usually 
contain,  also,  some  lime,  which,  with  the  interstratified  limestone,  adds 
a  calcareous  ingredient.  The  other  has  its  origin  in  the  arenaceous 
shales,  which  give  rise  to  a  somewhat  sandy  soil.  The  two  mingle 
for  the  most  part,  producing  an  intermediate  and  excellent  soil.  In 
portions  of  the  towns  of  Ottawa,  Eagle,  Palmyra,  and  La  Grange, 
however,  the  sandy  element  is  objectionably  prevalent. 

The  decomposing  shales  are  used  in  the  manufacture  of  brick,  of 
which  they  make  an  excellent  quality.  Some  of  the  clays  of  this 
formation  possess  an  exceptionally  fine  texture,  and  are  much  freer 
from  sand,  or  grit,  than  most  drift  clays,  and  hence  are  to  be  recom- 
mended for  those  purposes  that  require  such  a  clay.  These  chiefly 
lie  in  the  upper  part  of  the  formation. 

It  may  be  remarked,  in  view  of  the  unwarranted  expenditures  that 
are  likely  to  be  made  under  false  advice,  or  superficial  knowledge,  that, 
however  much  any  portion  of  this  formation  may  resemble,  in  general 
aspect,  any  portion  of  the  Coal  Series,  there  never  has  been,  and  there 
is  no  likelihood  that  there  ever  will  be,  any  workable  deposit  of  coal 
found  either  in,  or  beneath  it.  No  reliance  whatever  is  to  be  placed  on 
the  physical  nature  of  the  rock.  The  fossils  found  in  it,  which,  in  this 
and  other  formations,  are  given  with  unusual  fullness,  demonstrate 
the  utter  folly  of  enterprises  looking  to  the  discovery  of  coal  in  or  be- 
neath this  formation. 

Distribution  and  Local  Details.  The  most  southerly  point  at  which  the  Cincinnati 
beds  have  been  observed  in  outcrop  is  near  the  middle  of  the  south  line  of  Sec.  9,  in 
the  town  of  Eagle,  Waukesha  county.  The  exposure  at  this  point  is  very  slight,  and 
consists  of  impure  limestone,  a  portion  of  it  having  an  earthy  and  a  portion,  a  granular 
crystalline  texture,  full  of  small  cavities,  and  speckled  with  ocherous  spots.  A  sufficient 
number  of  imperfect  fossils  are  present  to  determine  the  position  of  the  rock,  which  is 
near  the  upper  face  of  the  formation,  but  not  immediately  beneath  the  Niagara  lime- 
stone, there  being  a  bed  of  clay  or  clay-like  shale  between.  In  tliis  vicinity  the  drift 
contains  many  blocks  of  a  fine-grained,  dark  clay  shale,  and  a  lighter  colored,  olivaceous 
gray,  arenaceous  rock,  having  a  somewhat  shaly  structure.  The  two  kinds  are  not  un- 
commonly united  in  one  bowlder,  but  the  former  soon  disintegrates  on  exposure.  The 
slaty  portion  also  contains  many  comminuted  fragments  of  Lingula,  provisionally  iden- 
tified as  Lingula  Maquoketa,  and  of  indistinct  graptolitic  remains,  similar  to  Cliina- 
cograptus.  As  this  is  a  very  soft  rock,  and  the  blocks  are  little  worn,  and  are  essen- 
tially confined  to  this  vicinity,  where  the  glacial  moraine  crosses  the  Cincinnati  belt,  it 
is  safe  to  conclude  that  it  forms  one  of  the  members  of  the  Cincinnati  group  at  this 
point.  This  is  confirmed  by  the  fact  that  precisely  similar  rock  occurs  between  150  and 


THE  CINCINNATI  SHALES  AND  LIMESTONES.  3]  7 

175  feet  below  the  base  of  the  Niagara  limestone,  on  the  east  side  of  Lake  Winnebago, 
and  is  found  at  other  points,  constituting  a  portion  of  the  series. 

In  the  adjoining  section  (Sec.  10,  N.  W.  qr.),  the  Niagara  limestone,  which  consti- 
tutes Hinkley's  quarry,  rests  upon  a  dark  blue,  hard  clay,  constituting  the  upper  mem- 
ber of  the  formation.  The  transition  is  abrupt,  as  is  befitting  the  junction  of  the  Lower 
and  Upper  Silurian  formations. 

North  of  this,  the  formation  is  concealed  by  drift,  and,  except  as  occasionally  struck 
by  a  well,  is  not  again  accessible  to  observation  until  Roberts'  quarry,  on  the  south  side 
of  Pewaukee  Lake,  is  reached.  This  quarry,  like  the  last,  is  in  the  lower  beds  of  the 
Niagara  limestone,  and  has  for  its  floor  the  clay.like  shale  of  the  formation  under  con- 
sideration. Fortunately  for  the  geologist,  however  unprofitable  for  the  owner,  some 
"  experienced  miner,"  in  his  "  practical "  wisdom,  had  discerned  in  this  the  Coal  forma- 
tion (!),  and  expressed  the  belief  that  coal  would  be  found  beneath  the  shale;  so  a  shaft, 
was  sunk,  from  which  was  thrown  a  remarkable  abundance  of  beautifully  preserved  Low- 
er Silurian  fossils,  but,  it  is  needless  to  say,  no  "fossil  fuel."  The  shaft  and  boring  to- 
gether reached  a  depth  of  50  feet,  and  showed  an  alternating  succession  of  blue  shale, 
and  gray,  yellow,  and  blue  limestone,  associated  with  some  crystalized  quartz,  and  with 
considerable  iron  pyrites.  Among  the  fossils  collected  from  the  material  thrown  out  of 
this  shaft,  there  were  found  no  less  than  sixteen  species  of  Chaetetes,  nine  of  which  are 
regarded  as  new.  With  these  are  associated  two  species  of  Stellipora,  one  of  Dc- 
kayi,  two  of  Stictopora,  several  new  species  of  Trematopora,  a  Fenestella,  a  Retepora, 
an  Alecto,  and  two  of  Callopora,  making  nearly  thirty  species  of  Bryozoans  and  Corals. 
Of  other  forms,  there  were  found  five  species  of  Orthis,  six  of  Strophomena,  Crania  seti- 
gera,  Zygospira  modesta,  Pterinea  demissa,  Calymene  senaria,  an  Illcenus,  a  new  spe- 
cies of  Beyrichia  and  one  of  Ortonia.  These  all  came  from  the  upper  10  feet  of  the  shaft. 
Passing  onward,  the  formation  is  again  effectually  concealed,  till  the  town  of  Aship- 
pun  is  reached.  In  Sec.  6  of  this  town,  and  Sec.  1  of  the  adjoining  town  of  Lebanon, 
small  streams  have  denuded  arenaceous  beds  identical  with  the  rock  described  as  occur- 
ring in  the  drift  in  the  town  of  Eagle.  At  other  points  in  this  vicinity  the  presence  of 
the  formation  is  sufficiently  indicated,  even  though  it  does  not  display  itself  in  actual 
outcrops. 

At  Hartford,  these  shales  underlie  the  iron  ore  bed,  and  are  penetrated  by  cellars, 
wells,  and  other  excavations. 

The  portion  here  exposed  is  the  upper  stratum,  and  has  its  usual  characteristics,  being1 
a  blue,  clay-like,  fossiliferous  shale,  containing  some  limestone. 

The  following  list  of  fossils  will  be  of  local  interest:  Several  species  of  Chcetetes, 
among  which  are  C.  annuliferus,  C.  rhombicus,  and  a  new  species,  Stictopora  fragilis, 
Orthis  testudinaria,  0.  subquadrata,  0.  occidentalis,  Leptcena  sericea,  Strophomena  uni- 
costata,  Rhynchonella  capax,  and  some  undetermined  forms.  With  more  favorable 
exposures,  this  locality  would  doubtless  prove  prolific  in  interesting  species.  It  may  be 
remarked  as  a  practical  suggestion,  that  the  iron  ore  beds,  when  present,  always  lie 
above  this  formation,  except  where  disturbed  by  the  drift. 

Beneath  the  mines  at  Iron  Ridge,  and  in  the  vicinity  of  the  upper  portion  of  the 
formation,  is  a  light  greenish  blue,  scarcely  indurated  clay,  not  very  fossiliferous.  Be- 
low this  the  shale  is  darker  and  more  full  of  fossils.  As  usual,  interstratified  beds  of 
limestone  are  present.  The  upper  surface  of  the  clay  mingles  with  the  iron  ore  above 
for  one  or  two  feet,  rendering  it  too  impure  for  use. 

The  following  interesting  collection  was  made  at  this  point :  Chcetetes  rhombicus,  n. 
sn.,  C.  briareus,  C.  punctatus,  n.  sp.,  and  several  other  new  or  undetermined  species, 
Alveolites,  n.  sp.,  Aulopora  arachnoidea,  Alecto  inflata,  Stellipora  antheloidea,  Sticto- 
pora fragilis,  a  Helopora,  a  Lingula,  Orthis  testudinaria,  0.  lynx,  0.  subquadrata, 
and  an  undetrmined  species,  Strophomena  unicostata,  an  undetermined  Strepto- 


318  GEOLOGY  OF  EASTERN  WISCONSIN. 

rhynchus,  Leptcena  sericea,  Rhynchonella  capax,  and  a  new  species,  II.  perlamellosa. 
Beneath  the  ledges  in  this  region,  the  Cincinnati  beds  approach  near  the  surface,  but 
are  rarely  exposed  on  account  of  their  soft  nature.  It  is  to  this  fact,  chiefly,  that  the  ver- 
tical ledges  owe  their  origin.  The  soft  clays  and  shales  were  easily  carried  away  during 
the  drift  period,  leaving  the  firmer  Niagara  limestone  projecting  above.  Since  the  drift 
period,  the  springs  that  issue  so  numerously  at  the  surface  of  these  clays  have  worn 
them  away  still  farther,  and  the  limestone  from  above  has  fallen  in  huge  blocks  and  cov- 
ered the  slope  at  the  base  of  the  cliff.  So  that  not  only  in  the  region  we  are  now 
speaking  of,  but  for  a  hundred  miles  northward,  the  Cincinnati  formation  will  chiefly 
manifest  itself  by  a  slope,  covered  with  debris,  at  the  base  of  vertical  walls  of  limestone, 
known  in  all  this  region  as  "  The  Ledge."  Occasionally  streams  cut  through  this  loose, 
concealing  material,  and  display  portions  of  the  formation.  An  interesting  case  of  this 
kind  occurs  in  the  town  of  Herman,  where  a  beautiful  brook  tumbles  over  the  step- 
like  layers  of  Niagara  limestone,  and  finally  plunges  into  a  gorge  excavated  from 
the  shales  under  consideration.  Only  a  few  feet  of  blue  clay  and  a  yellow  arenaceous 
shale  are,  however,  exhibited.  A  similar  instance  occurs  in  the  N.  W.  qr.  of  Sec.  21, 
Taycheedah.  The  falls  at  this  point  wash  out  of  the  clay  large  numbers  of  aggrega- 
tions of  crystals  of  iron  pyrites.  These  ore  usually  globular,  but  sometimes  take  varied 
and  fantastic  forms.  A  considerable  deposit  of  travertine,  of  modern  origin,  occurs  at 
this  point. 

South  of  Clifton,  on  the  east  side  of  Lake  Winnebago,  upwards  of  175  feet  are  oc- 
cupied by  this  formation,  above  the  level  of  the  lake.  How  much  it  extends  below  is 
not  known.  The  upper  portion  is  chiefly  concealed  with  fallen  blocks  from  the  clift 
above  and  other  debris.  At  the  lake  level  there  appears  a  dark  chocolate  brown  shale, 
alternating  with  impure  limestone  and  shale  of  lighter  color.  The  dark  shale  contains 
many  comminuted  fragments  of  Lingulas. 

Above  this,  lies  a  bed  of  limestone,  about  eight  inches  thick,  of  mingled  crystalline  and 
earthy  structure.  Upon  this,  rests  a  dark  chocolate  brown,  slate-like  shale,  splitting 
with  facility  into  soft,  brittle  plates.  Many  water-worn  fragments  of  this  stratum  aro 
heaped  up  by  the  waves  on  the  beach  below,  and  present  an  exaggerated  illustration 
of  the  difference  between  the  rounding  effects  of  beach  action  and  of  running  water . 
In  the  former  case,  the  effect  of  the  waves  is,  to  cause  the  fragments  to  move  up  and 
down  the  sloping  beach,  and  if  they  were  originally  flat,  as  in  this  case,  their  tendency 
is  to  slide,  rather  than  roll,  and  the  result  is  a  round,  disk-like,  but  not  globular,  form, 
and  this  is  very  markedly  the  case  at  this  point.  On  the  other  hand,  the  effect  of  run- 
ning water  is  to  roll,  rather  than  silde,  the  fragments,  and  hence,  to  produce  spherical 
pebbles.  This  distinction,  may  be  studied  with  profit,  in  connection  with  the  drift  de- 
posits. Above  the  slate-like  beds,  lies  a  yellowish  gray  shale  of  homogeneous,  some- 
what arenaceous  texture,  and  having  a  conchoidal  fracture,  giving  the  rock  the  appear- 
ance of  having  an  obscure  concretionary  structure. 

Beds  higher  than  these,  and  lower  than  those  previously  described,  are  slightly  ex- 
posed in  Lot  59,  Stockbridge,  where  shales  and  limestones  constitute  the  section  and  Orthis 
occidentalism  0.  tricenaria,  Strophomena  alternate,  and  Rhynchonella  capax,  the  chief 
features  of  the  fauna.  An  extraordinarily  large  specimen  of  the  last  named  species  was 
found,  by  Mr.  King,  at  this  locality.  In  Brown  county,  several  of  the  streams  that 
come  down  from  above  the  ledge  denude,  to  some  extent,  the  Cincinnati  beds.  One  of 
these  forms  the  beautiful  Cascade  Falls,  east  of  De  Perc,  where  the  shales  underlie  the 
iron  ore  deposit,  and  will  be  again  mentioned  in  connection  with  that  formation,  and 
another,  east  of  Green  Bay,  forms  a  succession  of  rapids  over  greenish  blue  shales  and 
limestones. 

On  reaching  Green  Bay,  the  formation  is  better  exposed  in  its  upper  portion,  but  its 
base  here,  as  elsewhere,  is  concealed.  The  escarpment  of  limestone  that  forms  Whit- 


THE  CINCINNATI  SHALES  AND  LIMESTONES.  319 

fley's  Bluff  is  underlaid  by  about  65  feet  of  this  formation,  consisting,  so  far  as  ex- 
posed at  the  time  of  examination,  mainly  of  blue  shale,  but  including,  also,  some  beds 
of  limestone.  A  portion  of  the  shale  consists  of  a  bluish,  drab-colored,  scarcely  indurated, 
clay,  of  very  fine  texture,  nearly  free  from  sand  and  similar  impurities,  and  is,  in  this 
respect,  much  superior  to  most  drift  clays,  and  is  worthy  of  attention,  as  an  excellent 
clay.  Crystals  of  gypsum,  of  the  variety  Selenite,  are  found  at  this  locality. 

North  of  this,  the  formation  is  quite  changeable  in  nature.  This  may  be  well  ob- 
served along  the  clitf  that  lines  the  shore  of  Green  Bay,  south  of  Little  Sturgeon  Bay. 
On  the  western  curve  of  the  point,  at  the  mouth  of  the  latter  bay,  where  the  formation 
last  displays  itself  in  force,  the  entire  exposure,  15  feet,  is  of  a  hard,  compact,  fine 
grained,  laminated  limestone,  showing  mud  cracks. 

Following  along  the  shore  southward,  a  most  interesting  series  of  minor  changes  and 
fine  exhibitions  of  the  manner  in  which  this  class  of  rocks  are  deposited,  is  presented  for 
study,  and  is  worthy  of  note  here  for  the  benefit  of  students  of  geology,  since  nowhere 
else  in  the  state  are  equally  good  opportunities  for  the  study  of  shale  deposits  afforded. 
Degrees  of  induration,  from  that  of  ordinary  clay,  to  rocks  of  almost  flint-like  hardness, 
varieties  of  lamination,  from  that  which  is  so  delicate  and  uniform  as  to  indicate  the 
most  quiet  depositing  waters,  up  through  various  degrees  of  undulation  and  irregularity, 
to  ripple  marks,  eight  inches  from  crest  to  crest,  and  an  inch  high ;  together  with  mud 
cracks,  so  pronounced  and  regular  as  to  sometimes  cause  the  surface  to  resemble  a  pave- 
ment of  octagonal  bricks,  may  be  observed,  while  the  cliffs  are  banded  and  variegated 
with  various  shades  of  blue,  green,  gray  and  purple,  the  whole  indicating  great  variety 
of  conditions  and  of  material,  within  a  limited  area. 

The  formation  is  here  much  more  calcareous  and  more  firm  and  resisting  in  its  nature, 
and,  at  the  same  time,  less  fossiliferous  than  at  any  point  observed  to  the  southward.  In 
some  of  the  lower  layers  exposed,  there  is  much  chert  in  large  nodular  or  lenticular 
masses. 

The  following  section  is  perhaps  as  nearly  typical  as  any  that  could  be  selected  to  rep- 
resent the  formation  at  this  extremity  of  its  area : 

1.  Hard,  fine  grained,  compact,  argillaceous  limestone,  in  beds  10  inches 

or  less  in  thickness,  some  of  them  weathering  rough  and  irregular. 
About 9  ft. 

2.  Similar,  but  harder  limestone,  marked  with  undulating  and  contracted 

laminations;  some  shaly  layers  interstratified;  bluish  gray  in  color, 

lined  with  red 7    ft.  6    in. 

3.  A  group  of  shales  of  varying  color  and  texture,  the  most  prominent  of 

which  are  finely  laminated  and  slaty,  splitting  up  on  exposure  into 
scales  and  plates,  while  some  are  more  clay-like.  The  group  in- 
cludes limestone  layers 16  ft.  8  in. 

4.  Thick  bedded,  blue,  cherty  limestone,  with  some  argillaceous  impurities 

in  the  form  of  laminse  and  partings 5    ft.  8    in. 

5.  Very  similar  to  the  above,  but  harder 1  ft.   1|  in. 

6.  Thin  bedded,  broken,  irregular,  nodular,  quite  eherty,  calcareous  layers. 

Exposed 3^  ft. 


Total,  about 44   ft. 


At  the  point  west  of  Little  Sturgeon  Bay,  the  formation  sinks  beneath  the  waters  of 
Green  Bay. 


320 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  TRENTON  PERIOD. 


GENERA  AND  SPECIES. 

5*3 

3 

m 

h 

Q 

1 

Lower  Blue. 

£ 
p 
M 
h 

V 

ft 

£ 

o5 

J3 

PQ 

§3 
s 

ft 

Trenton  Epoch. 

Galena  proper. 

Galena  modified. 

Cincinnati. 

PLANTS. 

* 
* 
* 
* 
* 
* 
* 
* 

* 

* 

* 
* 
* 

Buthotrcphis  succulcns  

* 

* 

* 

FORAMENIFERA. 

* 

* 
* 

* 

.... 

* 
* 

PETROSPONGIA. 

* 
* 

GRAPTOLITID^K. 

* 

* 
* 

* 

* 
* 
* 

* 

* 
* 
* 

* 

* 
* 
* 
* 

V 

* 
* 
* 

* 
* 

CORALS. 

* 

* 

* 

* 

* 

* 

* 

* 

* 

.... 

... 

C     rhombicus   n    sp  

C     rugosus  

* 

* 

* 
* 
* 

* 

Monticulipora  Ralei  

StelliooraBolvstomella.  . 

* 

FOSSILS  OF  THE  TRENTON  PERIOD. 


321 


FOSSILS  OF  THE  TRENTON  PERIOD  —  continued. 


GENERA  AND  SPECIES. 

«tt 

3 
PQ 

h 

I 

o 
3 

K 

H 

O 

1 

5*3 

3 

m 

Z 

x> 

p< 

P 

o5 

3 

3 

£l 

a 

& 

& 

4 

o 
A 
W 
g 
-S 

1 

Vl 

o> 
p. 
p 

£ 

cS 

1 

0 

Galena  Modified. 

Cincinnati. 

CORALS  —  con. 

* 

Alveolites   n   sp    

* 

* 

Streptela^ma  (Petraia.)  corniculum  .    ... 

* 

* 

* 

* 

S.     (Zaphrentis)  multilameUosum  

* 

* 

S     urd  sp  

* 

* 

Columnaria  s\.\  eolata   

* 

C     und  sp  . 

* 

Zaplirentis  und  sp  

* 

* 

Coral  resemb  Calceola  

* 

Favosites   

* 

* 

CRINOIDEA. 

Scluzocruius  nodosus  

* 

* 

* 

* 

Poteriocrinus,  und  sp  

* 

Cyathocrinus,  n.  sp    '^  

* 

Homocrinus,  und.  sp  

* 

Lidienocrinus,  sp.  ?  

* 

* 

* 

* 

CYSTID^EA- 

Pleurocystites  squaniosus  ?  

* 

* 

Glyptocystites  Logani,  

* 

BRYOZOANS. 

Treniatopora  sp.  res.  Gorgonia  peranticjua  .  .  . 

* 

* 

T.    new  and  und  species  

* 

* 

* 

* 

Stictopora  elegantula  

% 

* 

* 

* 

* 

1  ' 

* 

* 

S.    n.  sp.  No.  1  

* 

* 

* 

* 

S.    n  sp.  No  2  

* 

* 

S.    n.  sp.  No.  3  

* 

* 

Ptilodictya  recta  

* 

* 

* 

P.    und.  species  

* 

* 

Clathropora  flabellata  

* 

* 

Fencstella,  und.  sp  

* 

Alecto  inflata  

Aulopora  arachnoidea  

Helopora,  und.  sp  

Paleschara?  und.  sp  

BRACHIOPODA. 

Lingfula  alternata  

* 

9 

* 

* 

* 

* 

Wis.  SUR.  —  21 

322 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  TKENTON  PERIOD  —  continued. 


GENERA  AND  SPECIES. 

sw 
a 
« 

1 
& 

Lower  Blue. 

t 

m 
IH 

E 

B 

P 

Upper  Blue. 

f 

A 
S 

1 

1 

Galena  proper. 

Galena  modified. 

Cincinnati. 

BRACHIOPODA  —  (COH.) 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

0.    Ella  

* 

* 

* 

* 

0     lynx  

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

0     perveta  

* 

* 

* 

* 

* 

* 

* 

* 

• 

* 

0     subouadrata  

* 

* 

* 

* 

* 

* 

*  ' 

* 

* 

# 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

O     sp  res  0  hybrida  

* 

* 

* 

* 

* 

* 

* 

* 

Streptorhynchus  deflectum  . 

* 

* 

• 

* 

S.    deltoideum  

*9 

* 

* 

* 

S.     filitextum  

*? 

* 

* 

S     planunibonum    

*y 

* 

* 

* 

* 

* 

* 

* 

Strophomena  alternata  

* 

* 

* 

* 

* 

* 

* 

* 

* 

S.    camerata     

* 

* 

* 

* 

*? 

S.    camura  

* 

* 

* 

S.    incrassata  ... 

* 

* 

* 

* 

* 

* 

* 

S     recta  

* 

* 

* 

S     Thalia  

* 

S     n  sp  

* 

* 

* 

Strophodonta  

* 

* 

Leotasna  sericea.  . 

* 

* 

* 

* 

* 

FOSSILS  OF  THE  TRENTON  PERIOD. 


323 


FOSSILS  OF  THE  TRENTON  PERIOD  —  continued. 


GENERA  AND  SPECIES. 

Lower  Buff. 

<D 
9 

ffi 

1 

Upper  Buff. 

§ 

3 

i 

Trenton  Epoch. 

Galena  proper. 

Galena  modified. 

Cincinnati. 

BRACHIOPODA  —  (C0n.) 

* 

* 

* 

Z      recurvirostra  

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

LAMELLIBRANCHIATA. 

* 

* 

* 

A.    erecta  •  .-  

* 

* 

* 

* 

* 

* 

* 

A.    radiata  

*9 

* 

* 

A.    n.  sp.  

* 

* 

* 

* 

* 

T.    alta  

* 

T.    lirata  

* 

T.    levata  

* 

T     nasuta  

* 

* 

* 

* 

* 

* 

* 

* 

T.    n.  and  und.  sp  

* 

* 

Cypricardites  Canadensis  

* 

* 

C.    Niota  

* 

* 

* 

* 

* 

* 

C.    rotundatus  

* 

* 

* 

• 

* 

* 

C.    subtruncatus  

*? 

* 

* 

0     ventricosus  

* 

* 

* 

* 

* 

* 

* 

* 

• 

* 

C.     sp?...'.  

* 

Modiolopsis  f  aba  

* 

M.    plana  

* 

* 

* 

* 

* 

* 

M.    und.  and  n.  sp  

* 

GASTEROPODA. 

* 

* 

.  .  •  • 

* 

* 

* 

* 

* 

* 

* 

R.     Nasoni  

* 

* 

* 

Helicotonia  planulata  

* 

* 

* 

* 

* 

* 

* 

* 

Troclionema  arubisruum  

* 

* 

* 

* 

* 

T.    umbilicatum  

* 

* 

* 

* 

* 

* 

* 

T.    und.  sp  

* 

* 

324 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  TRENTON  PERIOD  —  continued. 


GENERA  AND  SPECIES. 

Lower  BufF. 

Lower  Blue. 

se 
P 
m 

b 

CD 

& 
Pi 

P 

o5 

3 

3 

b 
| 
1 

Trenton  Epoch. 

Galena  proper. 

Galena  modified 

Cincinnati. 

GASTEROPODA.  —  (con.) 

* 
* 
* 

p    Niota  

* 

* 

* 

.... 

* 

* 

.... 

* 

* 

X. 

* 

*9 

* 

... 

* 
* 

]VI     bellicincta^^M  major   :  

* 

* 



M     gracilis  

* 

* 
* 

* 

* 
* 

* 
* 

.... 

M     percarinata  ^  

* 

* 

* 
* 

M     tricarinata  

* 

* 

* 

.... 

M     three  n  sp  

* 
* 

* 

*9 

* 
* 

* 

* 



H     und    sp  

Subulites  eionsratus    

* 

* 
* 

* 

* 
* 

* 
* 

* 
* 
* 



Maclurea  Bigsbyi  

* 

* 

*9 
*' 
* 

M     camerata  n  sp  

M      subrotunda  n  sp  

* 

* 

* 

HETEROPODA. 

Bucania  bidorsata  

* 

* 
* 

* 

* 

* 

• 
* 
* 
* 

*  B     expansa  

B     punctif  ormis  

* 

B     und  sp  

* 

Bellerophon  bilobatus  

* 

... 

i    B.    ^Visconsinensis,  n    sp  •  

* 

* 
* 

* 

* 

* 
* 
* 

B      und  sp  

* 

C     Dyeii  

* 

* 

PTEROPODA. 

Conularia  Trentonensis  

* 

* 

* 

* 
* 

* 

Pterotheca  attenuata  

* 

.... 

* 
* 

E.    n.  SD  

* 

FOSSILS  OF  THE  TRENTON  PERIOD. 


325 


FOSSILS  OF  THE  TREXTOX  PERIOD  —  continued. 


GENERA  AND  SPECIES. 

£ 

I 

p 

m 
fe 

1 

3 

CQ 
53 

1 

| 

3 
PI 

1 

it 
i 

1 

Galena  proper. 

Galena  modified. 

Cincinnati. 

CEPHALOPODA. 

* 

0     anellum      

* 

* 

* 

* 

* 
* 

* 

* 
* 
* 
* 
* 
* 

* 

* 
*? 

* 
* 

* 
* 
* 

— 

* 
* 

0     planoconvexa     

0     vertebrate     .       

* 

* 

* 

.... 

* 

•v 

.... 

0.    n  sp  '^  

0     und  sp 

* 

* 

,,(_)     (Ormoceras)  Beloitense   n  sp      

* 

* 

Ornioceras  tenuifilum''*  

0     und  sp  

* 

* 

* 
* 

— 

Endoceras  annulatuni  ^    

* 

.... 

* 
* 

.... 

Cyrtoceras  annulatuni  

* 

* 

* 
* 

•v 

C     camuium  

* 
* 

* 
* 

— 

* 

C      und  sp  

* 

* 
* 

* 
* 

Oncoceras  Alceus  •       .       . 

* 

0.     abruptum  

* 

0.    Lycus  

* 

* 
* 

* 

.... 

O.    Pandion  

If 

0     plobeium  

.... 

* 

* 

0.    und  sp  

* 

.... 

Gyroceras  convolvans  

* 

* 
* 
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J&T    duplicostatum  n  sp  

Gonioceras  anceps  

* 

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.... 

.... 

Lituites  occidentalis  

* 

Gomphoceras  und  sp  

CRUSTACEA. 

Leperditia  fabulites  

* 

* 

* 

* 

Illsenus  crassicauda  ?  

* 

.... 

T     ovatus  

* 

* 

* 
* 

* 

* 

* 

* 

* 
* 

... 

* 

I 

* 

:;;; 

* 

* 

* 
* 

* 

Harpes,  und.  sp  

326 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OP  THE  TRENTON  PERIOD  —  continued. 


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GENERA  AND  SPECIES. 

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CLINTON  IRON  ORE  DEPOSIT.  327 


CHAPTER  YIEL 

UPPER    SILUBIAN. 

CLINTON  IRON  ORE  DEPOSIT. 

It  has  already  been  incidentally  stated,  that,  at  certain  points,  the 
Cincinnati  shales  were  overlaid  by  an  iron  ore  deposit,  while  much 
more  frequently  it  was  observed,  that  the  Niagara  limestone  rested 
directly  upon  them.  "Wherever  the  iron  ore  occurs,  it  is  found  to  be 
capped  by  Niagara  limestone.  The  phenomenon  presented,  then,  is 
that  of  a  separation  of  the  shales  and  limestone,  at  some  points,  by  a 
bed  of  iron  ore,  coming  in  between  them,  and  growing  thicker  till  its 
maximum  is  reached,  and  then  thinning  out  and  disappearing  again, 
forming  an  irregular  lens-like  mass. 

As  yet  there  seems  no  authentic  instance  of  organic  remains  having 
been  found  in  this  deposit,  although  I  was  shown  fossils,  said,  with 
undoubted  truth,  to  have  been  taken  from  the  ore,  but  they  were  pro- 
bably found  in  the  disturbed  drift  ore,  as  they  were  Cincinnati  species, 
specimens  of  which  were  ascertained  to  have  been  driven  up  by 
glacial  forces  into  the  mixed  mass  overlying  the  Mayville  ore  bed. 
"We  are  left,  then,  without  the  valuable  criterion  which  fossils  afford 
for  determining  the  age  of  this  important  formation.  But  there  is, 
nevertheless,  no  occasion  for  doubt  on  this  subject.  Its  stratigraph- 
ical  position  fixes  its  age  within  very  narrow  limits.  The  limestone 
above  belongs  to  a  very  low  horizon  in  the  Niagara  group,  and,  indeed, 
it  has  been  regarded  by  some  eminent  geologists  as  belonging  to  the 
Clinton  epoch,  and  it  probably  is  the  approximate  equivalent  of  the 
upper  portion  of  the  Clinton  beds  of  New  York,  but  as  will  be  seen 
hereafter,  there  is  no  good  reason  for  separating  this  limestone  from 
the  great  mass  of  the  Niagara  group,  with  which  it  is  intimately  con- 
nected. There  is  a  sharp  line  of  demarkation  between  the  ore  and  the 
limestone,  at  most  points,  so  that  there  is  no  reason  for  assigning  the 
ore  a  higher  position  than  the  Clinton  epoch. 

While,  as  already  stated,  the  clay  below  mingles  somewhat  with 
the  lower  layers  of  the  iron  deposit,  the  ore  "  takes  on  "  layers  at  the 
bottom,  so  that  its  beds  are  in  a  slight  degree  unconformable  to  those 


328  GEOLOGY  OF  EASTERN  WISCONSIN. 

below,  which  constitutes  a  reason  for  not  grouping  the  iron  beds  with 
the  Cincinnati  series. 

Within  the  limits  to  which  strati  graphical  evidence  thus  confines 
this  formation,  there  can  be  no  hesitancy  in  referring  it,  on  litholog- 
ical  grounds,  to  the  Clinton  epoch,  since  that  epoch  is  characterized 
from  Ohio  as  far  eastward  as  Nova  Scotia,  and  as  far  southward  as 
Alabama,  by  a  similar  deposit  of  oolitic  iron  ore. 

As  this  formation  is  developed  only  at  certain  localities,  we  may 
profitably  omit  further  general  remarks,  and  give  place  to  detailed 
local  descriptions. 

By  far  the  most  important  development  of  this  formation  occurs  at 
Iron  Ridge,  in  the  township  of  Hubbard,  Dodge  county.  The  main 
deposit  is  included  in  Sees.  12  and  13  of  that  town.  The  locality  is 
characterized  by  a  north  and  south  ledge  facing  the  west,  and  over- 
looking the  lower  land  in  that  direction,  from  a  height  of  about  sixty 
feet.  .  The  upper  twenty  feet  or  more  of  this  ledge  is  composed  of 
heavy,  rough  beds  of  Niagara  limestone.  Beneath  this  lies  the  ore 
bed  having  a  varying  thickness,  the  average  of  which  is  perhaps  fif- 
teen to  eighteen  feet. 

This  leaves  the  base  of  the  ore  at  a  most  convenient  elevation  above 
the  lower  land  adjoining  on  the  west,  giving  the  most  ample  facil- 
ities for  drainage,  loading  the  ore  into  cars,  or  supplying  the  ad- 
jacent furnace.  The  accompanying  topographical  map,  for  the  data 
of  which,  as  well  as  many  other  favors,  I  am  indebted  to  the  kind- 
ness of  Supt.  W.  C.  Sterling,  will  show  the  situation  more  precisely, 
and  the  chromo-lithograph  (PL  X),  which  has  been  accurately 
sketched  from  a  photograph,  will  give  a  more  vivid  conception  of  the 
relations  of  the  ore  and  the  method  of  mining,  than  can  be  conveyed 
by  description.  The  mine,  of  which  only  a  small  portion  is  shown 
in  the  plate,  is  situated  a  short  distance  west  of  the  center  of  Sec.  13. 

Near  it  is  the  furnace,  and  a  little  further  west  is  the  village. 
Three-quarters  of  a  mile  north  of  this,  is  the  Mayville  mine,  on  what 
is  known  as  the  Mayville  Ore  Bed,  though  the  village  of  Mayville  is 
four  miles  and  a  half  distant.  The  working  force  at  this  point,  at  the 
time  of  my  investigations,  was  in  charge  of  G.  K.  Hood,  to  whom  I 
am  indebted  for  various  favors. 

Having  thus  before  us  the  essential  geographical  features  of  the 
location,  and  the  general  situation  of  the  ore  bed,  we  may  give  our  at- 
tention more  specifically  to  the  deposit  itself. 

The  ore  occurs  in  regular  horizontal  beds,  varying  from  about  3  to 
14  inches  in  thickness.  The  dip  is  slight  and  varying  in  direction. 
Near  the  furnace,  it  is  northward;  at  the  Mayville  Ore  Bed,  it  is  south- 


PLATE,  XI 


TOPOGRAPHICAL  MAP 

IROK  RIDGE  MIXIXO  PROPERTY 
Chiefty  fro/n  (tftta 


Snpt  ."W:  C. 

1873. 

^  /  irtfft.. 
Contour  Iirtes5  ft  .apart  i-frticrr//i/ 


T»r  MII.WA..KK,..  l.mi,,..\Kv.. 


CLINTON  IRON  ORE  DEPOSIT.  329 

eastward;  and  north  of  this,  it  is  again  northward.  This,  in  connec- 
tion with  the  fact  that  the  thickest  portion  of  ore  occurs  at  the  highest 
elevation,  near  the  center  of  the  deposit,  seems  to  indicate  that  appre- 
ciable, though  slight,  flexures  of  the  strata  have  taken  place  at  this 
point  since  their  original  deposition. 

FIG.  40. 


NORTH  AND  SOUTH  SECTION  THROUGH  THE  IKON  ORE  DEPOSIT,  IRON  RIDGE. 
1.  Cincinnati  Shale.    2.  Iron  Ore.    3.  Niagara  Limestone. 

The  ore,  as  a  whole,  must  be  classed  with  the  hematites,  although 
it  contains  a  notable  amount  of  water  in  combination,  and  gives  a 
streak  varying  from  a  dirty  red  to  a  yellowish  brown,  and,  except  the 
upper  layer,  which  differs  from  the  main  body,  seldom  gives  a  bright 
scarlet  streak  or  powder.  The  hydration  is  not  uniform,  however, 
and  is  most  marked  where  the  ore  is  most  exposed,  and  seems  to  be  a 
process  in  progress,  rather  than  an  original  characteristic.  The  water 
collected  in,  or  issuing  from,  the  mines  is  colored  to  a  bright  scarlet, 
although  a  spring  issuing  beneath  is  almost  free  from  indications  of 
iron,  as  indeed  are  all  the  springs  in  the  vicinity.  They  cannot  be 
relied  upon,  then,  to  indicate  the  presence  of  this  iron  deposit.  The 
ore  consists  chiefly  of  small  lenticular  concretions,  whose  average 
diameter  is  about  one  twenty -fifth  of  an  inch.  They  are  less  uniform 
in  size  than  would  appear  to  casual  observation,  being  of  all  dimensions, 
from  one  tenth  of  an  inch  in  diameter  to  those  that  are  very  minute. 
There  occur  also  in  all  of  the  layers,  but  more  numerously  in  the 
lower  ones,  larger  concretions  which  are  usually  more  or  less  lenticu- 
lar in  form,  though  frequently  otherwise.  These  seem  to  be  largely 
composed  of  argillaceous  material.  From  this  concretionary  or 
oolitic  structure,  the  ore  receives  its  popular  names,  "  seed  ore,"  and 
"shot  ore."  The  concretions  are  bound  together  by  just  enough  of 
adhesive  ore  powder  to  give  the  mass  a  somewhat  firm  coherence,  and 
the  result  is  a  soft,  granular  rock.  The  little  lens-shaped  concretions 
lie,  as  would  naturally  be  anticipated,  chiefly  upon  their  sides,  giving 
to  the  rock  a  ready  cleavage  in  a  horizontal  direction.  These  facts, 
together  with  the  vertical  joints  and  frequent  bedding  lines,  render 
mining  remarkably  easy.  The  prevailing  color  is  a  dark  reddish 
brown.  At  certain  points  it  becomes  purplish  and  even  bluish,  as  at 
the  Mayville  Ore  Bed,  where  the  term  "  blue  ore  "  is  applied. 

The  top  layer,  from  3  to  8  inches  thick,  differs  markedly  from  the 


330  GEOLOGY  OF  EASTERN  WISCONSIN. 

rest  of  the  deposit.  It  is  dark  purple  in  color,  much  harder  and  more 
compact  than  the  oolitic  ore,  and  is  not  lenticular,  though  sometimes 
incorporating  a  few  concretions.  It  gives  a  bright  scarlet  streak  and 
powder,  has  an  irregular  or  conchoidal  fracture,  and  much  higher 
specific  gravity  than  the  main  mass.  It  contains,  as  noted  by  Dr. 
Percival,  scales  of  specular  ore. 

At  the  mines,  the  bedded  ore  varies  from  15  to  25£  feet  in  thick- 
ness. To  this,  at  the  Mayville  Ore  Bed,  there  is  added  a  considerable 
depth  of  drift  ore  increasing  the  thickness  to  40  feet  or  more. 

FIG.  41. 
ft 


c 


.  ••;. .'\sja          ^^SfeS^g^gfegfeiga 


PBOFILB  SECTION  AT  THE  MAYVILLE  OKE  BED. 

a.  Cincinnati  Shale,    b.  Bedded  Ore.    c.  Drift  Ore.    d.  Niagara  Limestone,  Capping  Ore.  /.  Mixed 

Drift. 

The  accompanying  section  (fig.  41)  shows  very  inadequately  the  ar- 
rangement of  the  undisturbed  and  drift  ores,  and  of  the  ocherous 
drift,  gravel,  bowlders,  and  disturbed  and  undisturbed  limestone,  as 
seen  at  the  time  of  my  visits.  It  was  taken  just  when  the  drift,  in 
the  progress  of  mining,  was  giving  place  to  undisturbed  limestone,  a 
point  most  favorable  for  study.  It  will  be  noted  that  the  various 
bands  of  drift  material  extend  from  the  left  (north)  obliquely  upwards 
to  the  right,  and  that  at  the  left,  the  upper  dark  layer  of  ore  is  swept 
away,  and  at  the  right,  it  is  broken  up  in  a  peculiar  way  very  imper- 
fectly illustrated  in  the  figure. 

The  force  that  produced  the  disturbance  and  intrusion  of  the  ore 
into  the  common  drift  seems  to  have  come  from  the  west  of  north, 
and  to  have  been  massive  in  character.  It  is  but  another  characteris- 
tic instance  of  glacial  action. 

What  may  have  been  the  original  extent  of  the  ore  deposit  to  the 
westward  cannot  now  be  ascertained.  That  portion  lias  been  swept 
away  by  the  denuding  agencies  which  formed  the  valley  lying  in  that 
direction.  To  the  southward  and  south-westward,  the  same  agencies 
have  limited  our  knowledge.  To  the  eascward,  the  deposit  thins  out. 
To  the  northeastward,  there  rises  a  high  ridge,  underlaid  by  a  consid- 
erable depth  of  limestone,  which  has  thus  far  limited  explorations  in 
that  direction,  since  the  immense  quantities  of  ore  already  developed 
leave  no  necessity  for  further  exploration  at  present  by  the  company 


CLINTON  IRON  ORE  DEPOSIT. 


331 


owning  the  land.  The  deposit  may  be  traced  a  mile  and  a  quarter  to 
the  northward  from  the  furnace,  where  it  is  lost  unde^  the  hills  that 
rise  in  that  direction.  It  has  been  found  in  a  thin  deposit,  two  milos 
farther  on  to  the  west  of  north,  in  the  town  of  NVilliamstown.  It  has 
also  been  found  a  mile  to  the  east  of  the  furnace.  Though  it  is  dim- 

O 

cult  to  give  even  an  approximate  estimate  of  the  amount  of  ore  here 
deposited,  it  is  at  least  safe  to  say  that  it  is  to  be  reckoned  by  millions 
of  tons,  and,  though  not  absolutely  inexhaustible,  is  at  least  adequate 
to  all  anticipated  wants  for  a  long  period  to  come. 

Both  open  and  underground  mining  have  been  made  use  of,  but 
the  former  method  has  been  found  the  most  economical. 

The  position  of  the  ore,  outcropping  along  the  face  of  a  terrace,  at  a 
convenient  elevation,  rendering  drainage,  "  stripping,"  loading  into 
cars,  or  the  furnace,  convenient,  the  soft  character  of  the  ore,  its  hor- 
izontal bedding  of  medium  thickness,  the  ease  with  which  it  may  be 
bored  and  blasted,  its  situation  in  a  rich  agricultural  arid  heavily  tim- 
bered region,  and  its  railway  connections,  combine  to  render  this  lo- 
cality unsurpassed  in  the  advantages  it  presents  for  mining,  reducing 
and  shipping  the  ore. 

The  following  table  of  analyses  shows  the  chemical  nature  of  the 
ore: 


t-t 

a 

o> 

O 

8 

S"E 

PQ 

pq 

<o 

ANALYSES  OP 
IRON  RIDGE  ORE. 

1 

£ 

g"0 

fi    O 

w 

•  P< 

S-t 

9 

4| 

—  O 

at 

'm    O> 

H 

?! 

£% 

o_"« 
oil* 

GO     ^ 

CO    — 

|| 

l-s 

PQ 

« 

PQ' 

t-iS 

PQ 

m 

PQ 

pq 

Loss  by  heat  at  212°  

2.00 

3.00 

2.00 

Specific  gravity  

2.94 

3  07 

2  99 

0  0'-* 

Peroxide  of  iron  

72  .  50 

74  40 

79  25 

76  74 

77  34 

78  75 

41    fi7 

r-p  '  -J 

Carbonate  of  lime  

0.56 

6.72 

6.81 

0.55 

2.00 

15.48 

0.75 

Carbonate  of  magnesia.  .  .  .'  

0.64 

0.41 

0.14 

6.64 

trace. 

8.25 

trace. 

Oxide  of  manganese  

1.40 

i.05 

3.50 

3.30 

2.56 

3.10 

Alumina  

8.40 

2.26 

2  49 

4  00 

5  00 

4  50 

19  74 

K.    91 

Silica  

7.75 

9.11 

6  18 

10  09 

8  57 

6  40 

15  19 

10  1° 

Water  and  loss  

8.75 

3.10 

4.00 

2.65 

2.65 

Water  

6.00 

3.00 

4.30 

Loss  

2.22 

1  30 

Phosphoric  acid  

1.00 

1.13 

2.75 

0.75 

1.53 

100. 

100. 

100. 

100. 

100. 

100. 

100. 

100. 

Metallic  Iron  

54.14 

54.13 

29.17 

53.56 

In    his  report,  Dr.  Jackson  says,  that  the  lime  and  magnesia  are 
combined  with  the  silica  and  not  with  carbonic  acid,  so  that  the  above 


332  GEOLOGY  OF  EASTERN  WISCONSIN. 

table  should  read,  lime,  for  carbonate  of  lime,  and  magnesia,  for  car- 
bonate of  magnesia,  so  far  as  his  anslysis  is  concerned. 

I  am  indebted  to  the  kindness  of  Supt  Sterling,  for  the  following 
relating  to  the  iron  interest  at  this  point.  The  whole  amount  of 
ore  shipped  from  July  1,  1869,  to  January  1,  1872,  was  173,842  tons; 
the  amount  in  1872,  82,371  tons;  in  1873,  48,706  tons;  total  for 
the  three  and  a  half  years,  304,919  tons.  This  ore  was  shipped  to 
Chicago,  Joliet  and  Springfield,  111.,  St.  Louis,  Mo.,  "Wyandotte  and 
Jackson,  Mich.,  Appleton,  Green  Bay  and  Milwaukee,  in  our  own 
state,  and  Zanesville  and  Newburg,  Ohio,  as  well  as  to  various  other 
points  in  small  quantities. 

The  cost  of  mining  the  ore  (1873)  is  from  50  to  75  cents  per  ton. 

The  value  of  the  ore,  delivered  on  the  cars,  is  from  $1.50  to  $2.00  per  ton. 

The  average  furnace-yield  of  metal,  from  the  ore,  is  45  per  cent. 

The  furnace  at  this  point  is  40  feet  high,  9^  feet  across  the  boshes, 

uses  4  or  5  tuyeres,  as  occasion  may  require,  makes  use  of  the  hot  blast, 

blown  by  steam  power,  burns  charcoal  —  the  average  cost  of  which  is 

11|-  cents  per  bushel  — and  has  a  capacity  of  about  3,500  gross  tons 

yearly.     No  flux  is  used. 

The  composition  of  the  pig-iron  product  is  shown  by  the  following 
analysis,  by  E.  T.  Sweet,  kindly  furnished  by  Prof.  Irving: 

Per  cent. 

Iron 95.784 

Phosphorus 1 .675 

Graphite 1.379 

Combined  carbon » 0.849 

Silicon 0 . 491 

Sulphur 0.108 

Manganese Trace. 

100.286 


In  1849,  a  blast  furnace  was  established  at  the  village  of  Mayville 
for  the  reduction  of  this  ore.  I  am  indebted  to  Mr.  James  Secular 
for  the  following  facts  concerning  its  present  capacity  and  workings 
(1873):  Height,  forty  feet  —  nine  feet  in  the  boshes;  uses  four 
tuyeres,  the  hot  air  blast,  charcoal  as  fuel,  and  steam  and  water  com- 
bined, as  power.  The  charge  is  seven  hundred  pounds  of  ore  and  six- 
teen bushels  of  charcoal.  The  ore  used  is  from  the  north  opening  at 
the  Mayville  Ore  Bed.  Limestone  and  lean  ore  have  sometimes  been 
used  as  a  flux.  Sandstone  was  being  tried.  The  yield  is  thirteen  or 
fourteen  tons  of  iron  per  day,  being  about  forty -two  per  cent,  of  the  ore. 

Hartford.  The  deposit  at  this  place  is  altogether  similar  to  that 
at  Iron  Ridge.  It  is,  however,  much  inferior  in  both  vertical  and 
lateral  extent,  and  if  the  numerous  statements  collected  concerning 


CLINTON  IRON  ORE  DEPOSIT. 


333 


the  wells  of  the  place,  with  such  observations  as  were  possible,  can  be 
trusted,  much  more  uneven.  The  bed  underlies  the  southeastern  por- 
tion of  the  village.  In  the  southwestern  portion,  the  denuding  agen- 
cies have  swept  away  the  overlying  limestone  and  the  ore,  if  it  ever 
existed  there,  and  have  substituted  adrift  deposit.  On  the  north  side 
of  the  Rubicon,  the  horizon  of  the  ore  has  been  depressed  by  an  ap- 
parent fault,  so  as  to  occur  at  a  considerable  depth  below  the  surface 
of  the  river.  There  seerns  good  evidence  that  the  deposit  reaches  ten 
or  twelve  feet  in  thickness  at  some  points,  but  rapidly  thins  out,  so 
that  the  average  thickness  for  the  area  over  which  it  occurs  probably 
does  not  exceed  two  feet.  The  accompanying  section  will  show  the 
general  nature  of  the  deposit  and  its  relations. 

FIG.  42. 


Jf.X. 


POSITION  AND  RELATIONS  OP  THE  IRON  ORE  AT  HARTFOKD. 
N-  L.  —  Niagara  Limestone.    C.  8.  —  Cincinnati  Shale. 

Besides  the  deposits  at  Iron  Ridge  and  Hartford,  and  their  vicinity, 
drift  ore,  of  precisely  similar  nature,  occurs  in  the  town  of  Stockbridge. 
The  deposit  is  small  and  lies  upon  the  west  side  of  a  ridge  of  moder- 
ate height,  the  exterior  of  which,  at  least,  is  drift.  A  well  in  the 
vicinity  is  said  to  have  reached  iron  ore,  eighteen  inches  in  thickness, 
beneath  limestone. 

At  the  Cascade  Falls,  east  of  De  Pere,  the  formation  again  appears. 
Its  situation  beneath  the  Niagara  limestone  and  above  the  Cincinnati 
shales  is  shown  in  the  accompanying  figure.     The  fall 
is  caused  by  the  fact  that  the  iron  ore  is  more  easily 
worn  away  by  the  action  of  the  stream  than  the  lime- 
stone above.     The  shale  is  somewhat  more  resisting 
than  the  ore.     The  maximum  thickness  of  the  ore  is 
five  feet.     On  the  east  side  of  the  gorge,  its  base  was 
c  concealed  at  the  time  of  examination,  and  it  was  only 
at  the  fall,  and  to  the  west  of  it,  that  fnll  measurements 
_a  could  be  made.     Just  east  of  the  fall,  the  thickness, 
measured  as  accurately  as  the  nature   of   the   case 
ADE  FALLS,  NEAR  would  admit,  is  four  feet,  eight  and  one-half  inches. 
Just  west  of  the  fall  it  is  four  feet  nine  inches.     A 

a.  Cincinnati  shale.      Viii     £     it.  \  ±1  n       j?    ^i 

b.  Clinton  iron  ore.      httle  farther  on  where  the  wall  of  the  gorge  curves 

c.  Niagara  limestone,  toward  the  north,  it  reaches  its  maximum  of  five  feet. 


FIG.  43. 


334:  GEOLOGY  OF  EASTERN  WISCONSIN. 

and  still  farther  on,  it  is  reduced  to  four  feet  six  and  one-  half  inches. 
Near  the  point  of  greatest  thickness,  there  are  slight  indications  of 
"taking  on"  layers.  The  ore  at  this  point  is  very  similar  to  that  at 
Iron  Ridge.  The  oolitic  concretions  are  somewhat  larger  on  the  aver- 
age, and  of  a  slightly  duller  color,  and  there  is  a  greater  amount  of 
argillaceous  material  present.  Upon  the  bed  of  lenticular  ore,  there  is 
a  highly  pyritiferous  layer  that  seems  to  represent  the  dark  layer  at 
Iron  Ridge.  Along  the  shore  of  Green  Bay,  south  of  Little  Sturgeon 
Bay,  this  geological  horizon  is  marked  by  a  somewhat  continuous  bed 
of  ore,  or  ocherous  rock,  of  a  few  inches  thickness.  It  very  rarely  pre- 
sents an  oolitic  structure,  or  other  characteristic  of  the  deposits  already 
described,  but  it  is  identical  with  them  in  geological  position,  and 
must  be  regarded  as  their  stratigraphical  equivalent. 

It  appears,  then,  from  the  foregoing  facts,  that  this  iron  ore  occurs 
at  widely  separated  points,  and  that  between  these  it  is  entirely  want- 
ing, or  is  represented  only  by  a  rusty  seam  between  the  limestone  and 
shale.  There  can  be  no  doubt  that  it  was  a  marine  deposit,  for  in  ad- 
dition to  the  evidence  of  the  beds  in  this  state,  the  equivalent  forma- 
tion elsewhere  contains  the  remains  of  marine  life.  It  appears  alto- 
gether probable  that  the  ore  was  deposited  in  detached  basins,  over 
which,  and  over  all  the  intervening  region,  the  Niagara  limestone  was 
afterwards  laid  down,  enclosing  the  detached  deposits  between  it  and 
the  shale  below  in  the  form  of  lenticular  masses.  This  ore  is  to  be 
sought  for  only  between  the  Cincinnati  shales  and  the  Niagara  lime- 
stone. The  line  along  which  the  junction  of  these  two  formations 
comes  to  the  surface  wrill  be  found  traced  with  much  care  on  the 
accompanying  maps.  To  the  east  of  this  line,  the  horizon  of  the  ore 
lies  beneath  the  Niagara  limestone,  and,  so  far  as  geological  evidence 
goes,  is  as  likely  to  be  found  at  the  base  of  that  formation^,  at  any 
point  over  the  broad  area  occupied  by  it,  as  at  the  points  where  its 
base  has  come  to  be  exposed  at  the  surface  by  denuding  agencies.  Of 
course  the  value  of  a  bed  of  ore,  found  at  any  considerable  depth  below 
the  surface,  would  be  very  seriously  affected  by  its  unfavorable  po- 
sition. 

While  it  is  probable  that  beds  of  this  ore  do  exist  at  points  not  yet 
discovered,  it  is  prudent  to  bear  in  mind  that  deposits  of  the  thick- 
ness of  that  at  Iron  Ridge  are  very  rare,  there  being  but  a  single 
known  instance  of  a  thicker  deposit  in  all  the  wide  range  of  the  Clin- 
ton formation,  though  beds  of  less  depth  are  profitably  mined;  and 
while  it  is  legitimate  to  hope  that  further  profitable  discoveries  may 
yet  be  made,  it  is  the  part  of  wisdom  to  exercise  due  caution  in  the 
expenditure  of  time  or-  funds  in  exploration,  and  to  be  guided  by  an 


PLATE.Xffi 


NIAGARA  LIMESTONE.  335 

intelligence  derived  from  careful  study  of  the  geological  facts  relating 
to  this  interesting  formation. 

NIAGARA  LIMESTONE. 

The  shales  and  iron  ore  deposits,  that  have  last  been  described,  lie 
along  the  eastern  margin  of  the  great  Green  Bay  and  Rock  river  val- 
ley, and  are  to  a  large  extent  overhung  by  beetling  cliffs  of  craggy 
limestone  that  form  the  western  projecting  edge  of  the  Niagara  for- 
mation. 

The  strata,  that  thus  jut  out  along  this  border,  form  the  lower  mem- 
ber of  an  extensive  and  important  limestone  group,  that  occupies 
nearly  all  the  region  between  this  border  and  Lake  Michigan.  The 
strata  dip  to  the  eastward,  so  that  the  higher  members  of  the  series 
appear  in  succession  in  that  direction.  All  these  members  are  mag- 
nesian  limestones,  or  dolomites,  some  of  them  being  among  the  purest 
known. 

The  belt  occupied  by  this  formation  has  a  north  and  south  extent 
of  about  two  hundred  miles.  In  the  course  of  this  extension,  its 
character  undergoes  a  change,  so  that  its  nature  at  the  two  extremi- 
ties is  quite  different.  And  it  is  a  most  interesting  fact  to  note  that 
this  change  takes  place  at  the  same  latitude  as  that  at  which  the 
changes  that  we  have  previously  noted  in  the  lower  formations,  espe- 
cially the  Galena  limestone,  take  place.  At  the  north,  there  are  six 
subdivisions,  sufficiently  well  marked  and  persistent  to  justify  their 
being  named,  described,  and  mapped  separately.  At  the  south,  there 
are  four  such  subdivisions.  It  should  be  observed  that  these  are  de- 
nominated subdivisions  of  the  Niagara  limestone.  They  are  not  re- 
garded as  distinct  formations,  or  as  having  the  grade  of  epochs,  as  that 
term  is  usually  understood,  but  they  are  nevertheless  well  character- 
ized subordinate  divisions  of  a  formation  of  more  than  ordinary  im- 
portance, and  it  is  believed  to  be  of  much  value  to  industry,  as  well 
as  science,  to  give  all  the  exactness  and  precision  possible  to  its  inves- 
tigation and  description.  The  names  given  to  the  subdivisions  are  as 
follows,  placed  opposite  to  each  other  for  convenience  of  comparison: 

NIAGARA  GROUP. 

At  the  South  —  At  the  North  — 

1.  Guelph  Beds.  1.  Guelph  Beds. 

2.  Racine  Beds.  2.  Racine  Beds. 

{3.  Upper  Coral  Beds. 
4.  Lower  Coral  Beds. 
5.  Byron  Beds. 
4.  Mayville  Beds.  6.  Mayville  Beds. 


830  GEOLOGY  OF  EASTERN  WISCONSIN. 

The  term  Guelph  has  been  applied  to  the  uppermost  beds  on  ac- 
count of  a  similarity  of  fossils  to  those  of  the  Guelph  limestone  of 
Canada,  to  which  the  Wisconsin  formation  is  probably  equivalent. 
The  recognition  of  this  equivalence  is  due  to  Prof.  "Whrtfield. 

The  Racine  beds  are  the  equivalent  of  what  has  been  known  as 
the  Racine  limestone,1  except  that  the  upper  portion  is  now  separated 
as  Guelph,  and  the  reefs  and  associated  rocks  west  of  Milwaukee, 
which  have  been  referred  to  a  lower  horizon,  are  included  in  it. 

.  The  lowest  strata  of  the  Niagara  series  are  named  'Mayville  beds 
because  they  have  their  maximum  development  and  linest  exposure 
south  of  that  village.  For  the  strata  that  lie  between  these  and  the 
Racine  beds,  in  the  southern  part  of  the  state,  the  term  Waukesha 
limestone,  which  has  been  previously  applied  to  a  portion  of  them, 
has  been  adopted  with  modifications.  The  white  limestone,  that  lies 
upon  the  Mayville  beds,  in  the  northern  portion,  receives  its  name 
from  the  township  of  Byron,  where  it  is  extensively  utilized  for  lime, 
building  stone,  and  flagging,  and  where  occurs  the  only  fossil  yet 
found  abundantly  in  it.  The  Upper  and  Lower  Coral  beds  have  been 
thus  designated  from  the  preponderance  of  coralline  forms  among 
the  fossils  found  in  them. 

The  accompanying  plates  (Plates  XII  and  XIII)  will  show  the  po- 
sition and  relations  of  these  subdivisons  very  satisfactorily.  Plate 
XIII  is  based  upon  the  facts  developed  in  sinking  the  Artesian  wells 
at  Sheboygan,  Milwaukee  and  Western  Union  Junction.  They  were 
sunk  after  my  investigations  upon  this  formation,  and  confirm  in  a 
most  satisfactory  manner  my  conclusions.  The  plate  also  illustrates 
a  number  of  other  interesting  geological  facts,  among  which  is  the 
northward  dip  of  the  strata.  It  also  furnishes  valuable  data  in  ref- 
erence to  Artesian  wells. 

MAYVILLE    BEDS. 

As  already  indicated,  these  beds  form  the  lowest  member  of  the 
Niagara  series  throughout  its  whole  extent.  They  possess  the  same 
general  character  throughout  their  entire  area,  and,  in  this  respect, 
differ  from  the  rest  of  the  group.  The  rock  of  this  member  is,  in 
general,  a  rough,  coarse,  gray,  magnesian  limestone.  There  is  consid- 
erable difference,  however,  among  the  several  layers  that  compose  it, 
and  some  of  these  maintain  their  peculiarities  with  great  persistency, 
so  that  it  is  possible  to  distinguish  them  at  points  one  hundred  miles 
or  more  apart.  This  makes  it  possible  to  describe  a  section  which 

Geology  of  Wisconsin,  1862,  p.  67. 


PLATE,Xn 


NIAGARA  LIMESTONE.  337 

will  be  applicable  in  a  general  way  to  the  formation  at  all  points,  and 
will  be  of  practical  service,  as  some  layers  are  valuable  and  others 
comparative!}7  worthless.  It  will,  however,  be  impossible  to  readily 
distinguish  all  these  layers  at  every  point. 

The  lowest  stratum  consists  of  from  four  to  ten  feet  of  shaly,  im- 
pure limestone,  usually  of  a  yellowish  gray,  but  sometimes  of  a 
greenish  hue.  The  beds,  at  some  points,  attain  sufficient  thickness 
and  soundness  to  be  serviceable  as  building  stone.  At  Iron  Ridge, 
this  stratum  either  disappears  or  loses  its  characteristics. 

Upon  this  lies  a  stratum  of  hard,  heavy-bedded  magnesian  lime- 
stone, usually  gray  in  color,  and  generally  characterized  by  prominent 
vertical  fissures  and  obscure  and  distant  bedding  joints.     It  does  not 
make  good  quicklime,  and  is  of  comparatively  little  value  as  a  build- 
ing rock.     It  varies  from  six  to  twelve  feet  in  thickness.     The  third 
general  stratum  is  composed  of  three  parts,  as  found  in  most  places. 
The  lower  one  consists  of  broken  fragments  of  limestone  imbedded 
in  a  greenish,  bluish  or  yellowish,  marly  clay.     More  or  less  of  chert 
is   present.     The   middle   portion   consists   of    compact,    sometimes 
cherty  limestone,  in  even  beds,  from  four  to  fourteen  inches  thick, 
and  serviceable  for  building  stone.     The  upper  portion  is  a  repetition 
of  the  lower.     The  three  portions  are  not  to  be  distinguished,  how- 
ever, at  all  points.     The  chert  is  sometimes  almost  entirely  wanting, 
as  in  Oakfield,  and  sometimes  is  a  very  prominent  feature,  as  in  Ot- 
tawa.    The  entire  stratum  varies  from  five  to  thirty-five  feet  in  thick- 
ness.    In  the  town  of  Taycheedah,  there  occur  at  the  bottom  of  this 
stratum  a  few  regular  beds  that  are  marked  by  an  abundance  of  Stro- 
matopora,   very  imperfectly  preserved.      They  should   probably   be 
grouped  with  the  above,  as    Stromatopora  extends  into  its  layers. 
This  stratum  is  overlaid  by  an  even  bedded  limestone,  usually  quite 
hard,  compact,  fine  grained,  white  or  light  gray,  often  nearly  a  pure 
dolomite,  and  a  valuable  rock.     At  the  same  horizon,  or  just  above  it, 
in  Taycheedah,  Empire,  Ashippun,  and  less  distinctly  at  some  other 
points,  there  occurs  a  reddish  yellow,  granular  crystalline  dolomite, 
called  by  the  workmen  and  residents  "  sandstone."     It  is,  in  fact,  an 
unusually  pure  dolomite,  so  that  if  the  term  is  understood  to  imply 
that  the  rock  is  silicious,  it  could  scarcely  be  more  erroneous,  since 
the  amount  of  silica  is  not  more  than  about  one-fourth  of  one  per 
cent.     It  is,  however,  a  fine  example  of  calcareous   sandrock.     The 
grains  are  chiefly  minute  crystals,  that  show  no  evidences  of  wearing 
action,  and  have  evidently  not  been  disturbed  since  their  crystalliza- 
tion.    The  interstices  between  the  crystals  are  to  a  considerable  ex- 
tent unfilled  by  any  matrix,  making  the  stone  highly  porous,  and,  in 
Wis.  SUR.— 22 


338  GEOLOGY  OP  EASTERN  WISCONSIN. 

some  cases,  rendering  it  liable  to  disintegrate  to  a  calcareous  sand. 
It  occurs  in  heavy  beds,  is  easily  quarried,  cuts  with  the  greatest  fa- 
cility, and  is  much  used  at  Fond  du  Lac  for  cappings,  etc.  It  is 
probable  that  this  and  the  preceding  rock  are  to  be  referred  to  the 
same  horizon,  as  they  seem  to  graduate  into  each  other  at  some  points, 
and  to  replace  each  other,  mutually,  at  others. 

Upon  this  rests  a  stratum  similar  to  the  second  in  being  charac- 
terized by  thick  beds  and  vertical  fissures,  but  differing  from  it  in 
being  less  hard,  and  in  possessing  a  highly  brccciated  structure  in 
some  localities.  To  the  position  just  above  this  is  to  be  referred  a 
layer  containing  many  obscure  casts  of  a  Pentamerus  (Gypidula\ 
very  similar  to  the  species  occidentalis.  This  stratum  is  succeeded 
above  by  the  white,  even-textured  limestone  of  the  Byron  and  Wau- 
kesha  beds. 

As  a  whole,  the  Mayville  beds  may  be  readily  recognized  by  their 
thick  bedding,  uneven  structure,  and  the  rough,  craggy,  pitted  sur- 
face of  the  weathered  ledges,  when  taken  in  connection  with  their 
position.  It  is  the  best  exposed  member  of  the  Niagara  group,  as 
it  forms  a  chain  of  craggy  cliffs,  upwards  of  a  hundred  miles  in 
length,  though  broken  down  and  concealed  at  frequent  intervals. 
The  greatest  observed  thickness  is  one  hundred  feet.  The  aver- 
age thickness  is  probably  not  more  than  sixty  feet.  The  chemical 
composition  of  some  of  the  more  important  of  these  beds  is  shown 
in  the  following  table : 

ANALYSES. 


I. 

...  50.52 

II. 
50.54 

III. 
53.95 

IV. 
55.03 

V. 
54.91 

VI. 
55.18 

...  40.97 

40.37 

44.28 

44.34 

42.77 

41.70 

...    0.77 

1.02 

0.30 

0.31 

0.43 

0.57 

...     3.49 

2.67 

0.10 

0.46 

0.18 

Si'lina 

.     3.57 

4.52 

1.23 

0.26 

1.35 

1.73 

\\rater  

...     0.48 

0.70 

trace. 

0.29 

0.26 

0.45 

Total 99.80        99.82        99.86      100:23      100.18        99.81 

Per  cent,  of  impurities 7.83         8.21          1.63         0.57          L>.^4         2.48 

The  rock  for  the  first  analysis  was  from  the  shaly  beds,  at  the  base 
of  the  formation,  that  are  used  for  making  waterlime  in  Williams- 
town  (N.  W.  1  of  N.  E.  J  of  Sec.  27,  T.  16  K,  K.  12  E.),  and  the  sec- 
ond was  from  similar  beds  found  in  Stockbridge  (1ST.  E.  J-  of  Sec.  11, 
T.  19  N.,  K.  18  E.).  The  third  was  from  the  limestone  used  at  the 
Appleton  iron  furnaces  for  flux,  and  obtained  from  the  lower  20,  feet 


NIAGARA  LIMESTONE.  339 

of  the  formation  at  Clifton,  on  Lake  Winnebago.  The  fourth  was 
from  the  so-called  sandstone  near  Taycheedah.  The  fifth,  from  the 
upper  layer,  aud  the  sixth  from  the  lower  layer,  at  Audley's  quarry, 
in  the  town  of  Delafield  (Sec.  20,  S.  E.  J).  The  limestone  in  the  last 
named  instance  included  many  nodules  of  chert,  which  were  excluded 
from  the  samples  analyzed,  one  object  of  the  analysis  being  to  ascer- 
tain the  chemical  nature  of  limestone  associated  with  well-defined  con- 
cretions of  chert.  The  above  analyses  were  executed  by  Prof.  Daniells. 

It  appears  that  in  all  cases,  the  carbonates  of  lime  and  magnesia 
exist  essentially  in  the  proportions  necessary  to  form  dolomite,  so  that 
these  beds  may  be  said  to  be  true  sedimentary  dolomites,  and  the  re- 
maining constituents  may  be  regarded  as  impurities,  and  are  so  sum- 
med up  for  convenience,  the  water  being  disregarded.  It  will  be  ob- 
served that  the  Taycheedah  "  sandstone  "  is  remarkably  pure.  This 
will  be  again  noticed  in  the  discussion  of  economic  considerations. 

Life.  The  remains  of  the  life  of  the  period  are  very  illy  preserv- 
ed, and  it  is  only  rarely  that  fossils  can  be  found  sufficiently  well-de- 
fined to  be  satisfactorily  identified.  In  most  cases,  only  obscure  casts 
remain.  It  is  not  to  be  inferred  from  this,  however,  that  the  life  of 
the  period  was  actually  meager.  On  the  contrary,  it  was  probably 
abundant.  The  conglomeritic  character  of  a  portion  of  the  beds  shows 
that  the  material  was  subjected  to  much  grinding  action  by  the  waves 
of  the  depositing  seas,  and  makes  it  probable  that  the  greater  portion 
were  comminuted  in  the  process  of  deposit,  while  the  crystalline  na- 
ture of  the  rock  suggests,  that  the  process  of  crystallization  may  have 
obliterated  some  that  escaped  comminution,  and  cavities  having  the 
form  of  fossils  show  that  some  others  have  been  removed  by  solution. 
From  the  nature  of  the  material,  some  of  the  identifications  are  neces- 
sarily doubtful,  and  are  so  indicated. 

In  the  following  table,  the  occurrence  of  the  several  species,  at  the 
more  important  localities,  will  be  found  systematically  and  compactly 
arranged.  Students  and  collectors  will  find  this  a  convenient  form. 
A  table  will  be  found  at  the  close  of  the  description  of  the  Niagara 
group,  in  which  the  fossils  of  this  member  are  compared  with  those 
of  the  other  beds,  which  will  also  be  found  instructive. 


340 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  MAYVILLE  BEDS  OF  THE  NIAGARA  GROUP. 


GENERA  AND  SPECIES. 

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* 

Economic  Value.  From  the  analyses  already  given,  it  will  be 
seen  that  some  portions  of  this  formation  are  remarkably  pure  dolo- 
mites, while  others  are  notably  impure.  From  the  description  already 


NIAGARA  LIMESTONE.  3-tl 

given,  and,  more  especially,  from  the  local  details  that  follow,  it  will 
appear  that  these  several  portions  occur  in  such  a  way  as  to  require 
some  discrimination,  if  the  best  quality  of  rock  is  to  be  chosen;  and 
it  is  hoped  this  report  will  furnish  some  assistance  in  making  a  suit- 
lable  selection. 

Kilns  for  the  reduction  of  lime  have  been  established  along  its  en- 
tire length.  These  vary  in  construction,  from  mere  rude  domes  of 
bowlders  to  approved  patent  kilns.  And  yet  some  of  each  class  were 
found  abandoned,  while  others  were  doing  a  profitable  business.  It 
was  observed  that,  in  many  cases,  an  impure  rock  had  been  burned. 
In  some  instances,  this  was  pardonable,  as  no  better  was-  exposed  in 
the  vicinity,  and  the  local  demand  warranted  the  use  of  such  as  was 
accessible,  until  improved  means  of  communication  supplied  a  supe- 
rior article  from  other  sources;  but  in  other  instances,  it  is  evident 
that  the  failure  was  due  to  the  use  of  inferior  rock,  when  a  superior 
ore  existed  in  the  immediate  vicinity. 

Properly  selected,  a  very  excellent  lime  may  be  made  from  this 
formation.  A  considerable  quantity  of  stone  may  be  selected,  in 
which  the  impurities  are  less  than  one  per  cent,  of  the  whole;  much 
additional  may  be  found,  in  which  they  are  less  than  two  per  cent., 
and  an  inexhaustible  quantity,  in  which  they  do  not  exceed  three  per 
cent.  The  large  percentage  of  magnesia  is  an  advantage,  for  it  is  a 
well  established  fact  that  dolomite  makes  a  stronger  cement  than 
simple  limestone.  At  many  localities,  the  better  class  of  rock  is 
used,  and  an  excellent  product  obtained.  Practical  suggestions  in  re- 
lation to  selection  will  be  found  in  Yol.  I,  where  they  are  given  to 
save  constant  repetition.  Numerous  statistics  relating  to  the  in- 
dustry were  taken ;  but  they  could  not  be  made  sufficiently  complete, 
accurate,  and  uniform  to  justify  publication  here. 

At  some  localities,  it  is  claimed  that  the  lower  beds  of  this  forma- 
tion are  suited  to  the  manufacture  of  hydraulic  lime,  and  analyses  I 
and  II,  given  above,  were  made  to  ascertain  upon  what  basis  this 
claim  was  founded.  The  composition,  it  will  be  seen,  is  quite  differ- 
from  that  of  the  celebrated  hydraulic  cements,  and  would  not  justify 
an  expectation  that  this  rock  would  produce  an  hydraulic  lime  that 
would  have  more  than  a  local  market.  It  will  doubtless  furnish  a 
serviceable  substitute  for  the  more  expensive  cements,  for  certain 
purposes,  \vhere  common  fat  lime  will  not  answer. 

Rock  obtained  from  Clifton  is  used  at  Appleton  as  a  flux  for  Lake 
Superior  iron  ores,  and  is  said  to  work  satisfactorily.  The  rock  is 
obtained  from  the  fallen  masses  on  the  slope  below  the  cliff,  which 
consist  of  a  mingling  of  the  several  strata.  The  analysis  above  given 


342  GEOLOGY  OF  EASTERN  WISCONSIN. 

represents  the  better  quality  found  in  the  rock  pile  at  the  furnace.  By 
comparison  with  that  from  Taycheedah,  it  will  be  seen  that  the  lime- 
stone used  is  not  the  purest  that  is  accessible  to  Lake  Winnebago,  and 
this  fact  may  be  worthy  of  the  attention  of  those  interested. 

For  the  purposes  of  ordinary  masonry,  this  formation  furnishes  an 
abundance  of  readily  accessible  material,  and  it  is  extensively  used 
for  such  purposes.  The  granular  stratum  furnishes  an  excellent  stone 
for  cutting.  Its  rich  cream  color  gives  it  a  very  pleasing  effect. 
Rock  obtained  east  of  Horicon  marsh  is  wrought  at  the  State  Prison, 
at  "Waupun,  and  quarries  have  been  opened  upon  this  stratum,  east  of 
Found  du  Lac,  from  which  a  supply  of  cut  stone,  for  that  city  and 
other  points,  is  obtained. 

Distribution,  and  Local  Descriptions.  By  consulting  the  maps, 
it  will  be  seen  that  these  beds  occupy  an  irregular  belt,  stretching  in 
a  nearly  north  and  south  direction,  from  the  Illinois  line,  in  Wai- 
worth  county,  to  near  the  extremity  of  the  peninsula  east  of  Green 
Bay,  where  it  dips  beneath  the  surface  of  that  body  of  water.  Most 
of  the  localities  here  mentioned  lie  on  the  extreme  western  margin 
of  this  belt,  and  show  the  projecting  edge  of  the  formation. 

The  point  at  which  the  formation  enters  this  state  from  Illinois,  or  leaves  it  in  that 
direction,  if  you  please,  is  deeply  concealed  by  drift,  but  there  is  abundant  reason  for 
believing  that  it  crosses  the  line  from  the  towns  of  Walworth  and  Linn,  as  represented 
on  the  map. 

On  the  north  side  of  Lake  Geneva,  the  limestone  approaches  the  surface,  but  does  not 
actually  outcrop.  The  most  southerly  point  where  the  western  limit  of  these  beds  is  ac- 
curately determined  by  outcrop  is  in  the  S.  W.  qr.  of  Sec.  10,  town  of  Eagle  in  Wau- 
kesha  county.  South  of  this  point,  the  outline,  as  mapped,  is  based  upon  topographical 
and  drift  evidence,  and  can  only  be  regarded  as  approximate.  At  Hinckley's  quarry,  in 
the  above-named  section,  four  feet  of  thin  bedded,  impure  magnesian  limestone,  having 
an  even  fracture  and  light,  yellowish  gray  color,  blotched  with  green  in  places,  espec- 
ially between  the  layers,  form  the  base  of  the  quarry,  and  rest  upon  the  Cincinnati  shale. 
Above  these  are  nine  feet  of  thicker  bedded  limestone  of  coarser  and  more  irregular  tex- 
ture, and  marked  by  walnut-sized  cavities,  lined  with  yellow  granular  matter. 

These  beds,  when  exposed  in  natural  ledges,  as  they  are  in  the  vicinity,  weather  to  a 
very  rough,  ragged  exterior,  due  to  the  irregularities  of  their  structure. 

In  this  region,  the  great  drift  moraine,  previously  described  as  the  Kettle  Range,  over- 
lies this  formation,  and  it  is  only  here  and  there  that  it  displays  itself.  Near  Hinckley's 
quarry,  the  lodge  swings  round  to  the  east,  and  disappears  beneath  the  drift  ridges.  It 
emerges  again  in  Sees.  11  and  14  of  the  town  of  Ottawa.  The  rock  here  is  char- 
acterized by  conspicuous  nodules  of  white  chert,  which  are  very  abundant  in  some 
layers. 

At  Hunter's  quarry  (Sec.  11,  S.  E.  qr.),  the  lower  three  feet  exposed  is  a  moderately 
hard,  compact,  gray,  magnesian  limestone,  marked  with  iron  stains.  Upon  this  lies  a 
somewhat  peculiar  shaly  layer,  which  may  be  described  as  chipstone  imbedded  in  a 
clayey  material.  Above  this  are  two  and  a  half  feet  of  more  solid  rock,  the  upper  por- 
tion of  which  is  cherty.  This  is  overlaid  by  another  shaly,  or  chipstone  layer,  similar  to 
that  below,  but  cherty;  and  this  in  turn  is  surmounted  by  a  few  rotten  buff  layers  that 


NIAGARA  LIMESTONE.  343 

complete  the  exposure.  The  two  chipstone  layers  are  worthy  of  note,  as  they  may  be 
recognized  more  than  a  hundred  miles  to  the  northward. 

In  Delafield,  the  next  town  north,  notwithstanding  the  drift,  the  formation  discovers 
itself  at  several  points,  though  nowhere  in  great  force.  Its  character  is  essentially  as  in 
Ottawa.  At  the  quarry  near  the  village,  the  two  shaly  layers  are  observable. 

At  Audley  and  Graham's  quarry  (S.  E.  qr.,  Sec.  20),  a  few  layers  of  dark,  gray 
crystalline  limestone,  containing  much  chert,  are  burned  for  lime.  The  analysis  of  this 
has  already  been  given.  At  Roberts'  quarry,  south  of  Pewaukee  Lake  (S.  W.  qr.  of  S. 
W.  qr.,  Sec.  24,  Delafield),  the  beds  are  more  close-textured  and  silicious  than  at  the 
points  previously  described,  and  the  chert  is  more  distinctly  arranged  in  layers  along 
the  bedding  joints.  The  exterior  of  the  layers  is  buff,  while  the  interior  is  blue,  the  lat- 
ter sometimes  appearing  as  a  well-defined  rectangle,  surrounded  by  a  border  of  buff', 
when  a  block  has  been  broken  across.  The  whole  was  undoubtedly  once  blue,  and  the 
buff  has  been  caused  by  leaching,  and  the  peroxidation  of  the  iron  present. 

The  formation  again  disappears  beneath  the  drift,  and  is  next  seen  in  the  town  of 
Ashippun,  in  Dodge  county,  where  it  forms  a  few  ragged  outlying  ledges.  The  most 
noteworthy  of  these  lies  in  the  west  half  of  Sees.  6  and  7.  It  rises  about  fifty  feet  above 
"  the  grade,"  at  its  base,  though  the  vertical  ledge  only  presents  a  face  of  about  twenty 
feet. 

The  bedding  joints  are  very  obscure,  and  the  layers  are  traced  with  difficulty,  so  that 
the  rock  presents  a  very  massive  appearance,  but  a  general  section,  somewhat  as  follows, 
may  be  made  out.  Six  feet  exposed  at  the  base  consist  of  a  hard,  but  porous,  dolomite 
of  uneven  texture,  made  up  of  fine  and  coarse  grained  patches,  mottled  gray  and  buff 
correspondingly.  This  is  overlaid  by  from  4  to  6  feet  of  very  hard,  compact,  flintliko 
limestone,  much  fissured  vertically.  Upon  this  rest  7  to  8  feet  of  a  reddish  buff,  gran- 
ular, somewhat  friable,  magnesian  limestone,  the  granules  consisting  of  small  crystals 
of  dolomite,  the  spaces  between  which  are  mostly  unfilled,  giving  a  porous  structure. 
Chemically,  this  is  a  very  pure  dolomite,  and  should  be  burned  for  lime  instead  of  either 
of  the  other  layers  exposed  at  this  point,  as  it  would  not  only  produce  a  superior  quality 
of  lime,  but  would  burn  easier.  This  is  undoubtedly  the  equivalent  of  the  "  sandstone  " 
layer  near  Taycheedah,  and  is  the  most  valuable  portion  of  the  beds  under  consideration. 
This  is  overlaid  by  6  feet  or  more  of  brecciated  rock,  consisting  of  subangular  fragments 
of  a  gray  magnesian  limestone,  imbedded  in  a  yellow,  granular  matrix  of  similar  chem- 
ical nature. 

North  of  this,  the  margin  of  the  main  body  of  the  formation  recedes  to  the  eastward 
as  far  as  Hartford.  Near  this  place  are  several  limited  exposures  of  these  beds,  one  of 
which,  on  the  farm  of  Mr.  Blodgett,  is  interesting  on  account  of  the  fossils  it  contains, 
a  list  of  which  has  already  been  given.  The  rock  is  a  light  colored,  granular  dolomite 
of  irregular  texture. 

Passing  by  several  outcrops  in  Herman,  we  find  at  Iron  Ridge,  reposing  on  the  ore- 
beds,  6  feet  8  inches  of  buff  magnesian  limestone,  in  beds  of  8  to  16  inches  thickness. 
Upon  this,  lies  a  layer  6  feet  8  inches  thick,  the  bedding  planes  of  which  are  very  obscure, 
so  that  it  appears  like  a  single  layer,  while  vertical  fissures  are  frequent.  This  is  over- 
laid by  2  feet  10  inches  of  thin  bedded  magnesian  limestone,  which  gives  place  above  to 
a  shaly  layer,  composed  of  rotten  chipstone,  mingled  with  a  greenish  blue  clay.  The 
whole  is  capped  by  about  6  feet  of  broken,  frost-riven  limestone.  As  the  mining  pro- 
gresses backward  from  the  face  of  the  ledge,  the  thinner  beds  will  doubtless  be  found 
uniting  into  thicker  and  more  solid  ones,  and  the  disintegrated  rock  will  give  place  to 
that  which  is  more  firm,  with  corresponding  changes  in  color  and  general  aspect. 

From  this  point  northward,  there  is  no  dearth  of  outcrops.  The  Kettle  Range  has 
receded  to  the  eastward,  and  there  is  left  only  the  usual  drift  deposit,  through  which 
the  formation  boldly  thrusts  its  jagged  edge. 


344  GEOLOGY    OF   EASTERN   WISCONSIN. 

About  two  miles  south  of  the  village  of  Mayville,  there  is  a  precipitous  cliff  100  feet 
in  hight,  exhibiting  the  full  extent,  and  more  than  the  usual  thickness  of  this  subdivision 
of  the  Niagara  group.  Owing  to  the  difficulties  of  measuring  on  the  vertical  face  of  the 
cliff,  the  thickness  of  the  beds  is  only  approximately  given  from  aneroid  measurement. 

At  the  base,  are  5  feet  of  the  usual  thin  bedded,  shelly,  light  colored  layers,  disinte- 
grated back  from  the  face  of  the  ledge. 

Overhanging  this,  is  12  feet  of  hard,  semi-translucent  dolomite,  not  separated  into  dis- 
tinct beds,  but  rifted  with  vertical  fissures,  which  do  not,  however,  extend  into  the  beds 
above  or  below.  This  supports  7  feet  of  shaly  and  cherty  rock,  lying  beneath  4  feet  of 
thick  bedded  limestone,  which  is  in  turn  overlaid  by  23  feet  of  shaly  and  cherty  layers, 
the  three  forming  the  shaly  or  chipstone  group,  previously  described. 

Upon  this,  lies  another  stratum  of  about  23  feet,  in  which  the  vertical  fissures  are  much 
more  pronounced  than  the  bedding  lines. 

This  is  surmounted  by  a  somewhat  thicker  group  of  soft,  white,  granular,  crystalline 
dolomite,  some  layers  of  which  contain  many  casts  of  fossils,  particularly  of  Gypiduhi. 
The  top  of  the  ledge  is  formed  of  white,  fine-grained,  crystalline  dolomite,  closely  re- 
sembling the  rock  of  the  next  group  above,  to  which  it  probably  belongs. 

In  crossing  the  east  branch  of  Eock  river,  the  boundary  again  swings  to  the  eastward 
as  in  the  case  of  the  Rubicon,  and  in  the  course  of  this  detour,  manifests  itself  in  several 
low  ledges. 

Returning  from  this  deviation,  the  formation  enters  upon  a  succession  of  precipitous 
ledges  that  extend  to  Little  Sturgeon  Bay.  These  are  all  so  like  each  other,  and  so  sim- 
ilar to  those  already  described,  that  it  will  not  be  necessary  to  repeat  the  details  of  their 
structure.  From  near  the  village  of  Kekoskee,  the  ledges  succeed  each  other  in  stair- 
like  order,  shifting  westward  till  the  margin  of  Horicon  Marsh  is  reached,  when  they 
stretch  northerly  to  its  extremity,  where,  forming  a  continuous  rampart,  the  line  curves 
rapidly  to  the  eastward  through  the  corner  of  Oakfield,  and  onward  hi  crenate  outline 
through  the  town  of  Byron. 

The  direction  of  the  ledge  is  now  in  the  line  of  dip,  and  the  beds  under  consideration 
rapidly  drop  down  and  are  soon  surmounted  by  the  white  walls  of  the  Byron  beds. 
Turning  abruptly  northward,  in  the  northwest  corner  of  the  town  of  Eden,  the  chain  of 
ledges  extends  through  the  western  part  of  Empire,  the  Mayville  beds  again  emerging 
and  forming  the  rocky  rampart,  while  the  white  Byron  beds  retire  to  the  eastward. 
Opposite  the  southern  extremity  of  Lake  Winnebago,  the  crown  of  the  cliff,  at  some 
points,  is  formed  by  a  very  pure,  granular  crystalline,  cream  colored  dolomite,  locally 
known  as  a  sandstone.  The  constituent  grains  are  small  crystals  of  the  carbonate  of  lime 
and  magnesia,  usually  quite  firmly  compacted,  but  sometimes  loosely  aggregated,  leav- 
ing numerous  interspaces,  which  render  the  rock  very  porous  and  disposed  to  crumble 
to  a  calcareous  sand,  whence  the  local  name.  It  is  probably  due  to  the  misapprehension 
of  its  real  character,  growing  out  of  the  use  of  the  name  sandstone,  that  it  has  not  been 
more  extensively  used  for  the  manufacture  of  lime,  instead  of  the  much  inferior  rock 
that  has  been  employed.  Aside  from  this  important  stratum,  the  formation  continues 
essentially  as  previously  described.  The  chain  of  cliffs  skirts  at  a  little  distance  the  east 
shore  of  Lake  Winnebago,  rising  more  than  200  feet  above  it.  Toward  the  northern 
extremity,  the  ledge  approaches  the  lake  and  directly  overlooks  it. 

Between  Lake  Winnebago  and  Green  Bay,  the  formation  is  more  broken  down  and 
covered,  but  on  reaching  the  eastern  shore  of  the  latter,  it  reappears  in  bold  relief,  crown- 
ing and  protecting  the  more  perishable  Cincinnati  shales,  and  giving  a  picturesque 
outline  to  the  bay  shore  as  far  north  as  Little  Sturgeon  Bay.  It  forms  the  rocky  sum- 
mit of  Whitney's  Bluff,  where  it  is  wrought  for  various  purposes.  The  most  northern 
place  where  it  is  extensively  used  is  on  the  shore  west  of  Little  Sturgeon  Bay,  where 
a  piei  and  kilns  have  been  constructed.  At  this  point,  many  of  the  general  features 


NIAGARA  LIMESTONE.  345 

noted  in  Waukesha  county  are  still  discernible  though  the  texture  and  composition  hera 
are  superior.  North  of  this  point  these  beds  drop  down  to  near  the  level  of  the  waters 
of  Green  Bay,  and  alternately  appear  and  disappear  with  the  undulations  of  the  strata, 
as  far  north  as  the  Light  House  point  opposite  Chambers'  Island,  where  they  finally 
disappear  beneath  the  waters  of  the  bay. 

BYRON  BEDS. 

Reposing  upon  the  coarse  textured  Mayville  beds  last  described, 
lies  a  somewhat  thicker  series  of  beds,  bearing  a  strong  contrast  to 
them  in  color,  texture,  stratification,  and  general  character.  The 
ledges  of  the  former  are  rough  in  aspect  and  dull  in  color,  those  of 
the  latter  are  usually  smooth  and  white.  The  texture  of  the  former 
is  generally  coarse,  and  often  very  uneven,  that  of  the  latter  is  always 
fine,  and  sometimes  so  close  and  compact  as  to  be  lithographic  in 
character.  The  transition  from  the  one  to  the  other  is  usually  ab- 
rupt and  well  defined.  These  facts  eminently  justify  the  distinction 
here  adopted. 

To  describe  somewhat  more  precisely,  it  may  be  remarked,  that  the 
color,  where  not  white,  is  a  light  gray  or  cream  tint,  sometimes  lined 
or  mottled  with  pink  in  a  very  handsome  manner.  The  texture  is 
usually  either  very  close  and  compact,  or  very  fine  grained.  In  the 
former  case,  it  is  hard  and  has  a  somewhat  glassy  fracture,  and  the 
edges  of  the  fragments  often  appear  translucent.  Such  portions 
often  have  a  grayish  water  hue.  The  other  class  usually  has  a  regu- 
lar or  conchoidal  fracture,  and  is  opaque.  Some  portions  are  finely 
laminated,  and  where  these  laminae  are  colored,  as  sometimes  occurs, 
a  beautiful  effect  is  produced. 

The  bedding  is  either  thin,  producing  excellent  flagging,  or  attains 
more  considerable  dimensions,  and  furnishes  cutting  and  building 
stone.  Some  of  the  strata  are  habitually  undulating,  and  some,  in  the 
weathered  ledges,  are  excessively  fractured  in  a  conchoidal  manner, 
while  others  are  vertically  fissured. 

Argillaceous  partings  are  occasionally  present,  and  the  rock,  though 
rarely,  becomes  shaly.  Mudcracks  and  ripple  marks  were  observed. 

The  following  analysis  of  rock  taken  from  Butler's  quarry  (Sec.  10, 
Byron),  made  by  Prof.  Daniells,  for  the  survey,  shows  it  to  be  a  near- 
ly pure  dolomite: 

Per  Cent. 

Carbonate  of  Iini3 54.25 

Carbonate  of  magnesia 44.48 

Sesquioxide  of  iron  .....' 0.26 

Sesquioxide  of  alumina 0.10 

Insoluble  residue 0 . 67 

Water 0.11 

Total .  99.87 


346  GEOLOGY  OF  EASTERN  WISCONSIN. 

Fossils.  These  are  very  rare.  At  Butler's  quarry,  in  the  town  of 
Byron,  Leperditia  fonticola  is  abundant,  this  being  its  typical  local- 
ity. Fucoidal  impressions  are  occasionally  met  with,  and  an  undeter- 
mined Zaphrentis  was  found  near  Sturgeon  Bay. 

Thickness.  The  greatest  observed  thickness,  not  including  the 
transition  beds  above,  is  110  feet;  including  that  portion  of  the  transi- 
tion beds  most  allied  to  this  division,  its  maximum  thickness  would 
reach  perhaps  140  feet. 

Distribution.  The  formation  presents  so  great  a  degree  of  uni- 
formity that  local  sections  and  descriptions  will  be  unnecessary. 

In  delineating  the  outcroppings  of  the  beds  below,  we  were  carried 
northward  to  near  the  extremity  of  the  peninsula  east  of  Green  Bay. 
We  may  secure  continuity  of  thought  and  save  ourselves  mental  trans- 
portation by  taking  up  the  distribution  of  this  division  at  that  point. 

It  was  stated  that  at  Little  Sturgeon  Bay,  the  Mayville  beds  dipped 
down  to  near  the  water's  edge.  On  doing  so,  they  are  at  once  sur- 
mounted by  the  Byron  beds,  in  fall  force.  These  form  a  series  of 
bold,  picturesque  cliffs,  extending  to  the  extremity  of  the  peninsula. 
Two  of  these  cliff's  stand  like  pillars  of  Hercules,  at  the  mouth  of  Big 
Sturgeon  Bay,  and  each  of  the  harbors  north  of  this,  on  the  west  side 
of  the  peninsula,  is  guarded  by  at  least  one  such  Cyclopean  sentinel, 
and  one  stands  by  Death's  Door  at  the  extremity.  South  of  Little 
Sturgeon  Bay,  this  formation  lies  a  little  back  from  the  rocky  escarp- 
ment that  faces  the  Green  Bay  valley,  and  its  strata  are  beveled  down 
to  the  general  surface  of  the  country,  so  that  it  displays  itself  less 
conspicuously.  The  belt  which  it  occupies  at  the  surface  lies  next 
east  of  the  Mayville  beds  as  far  south  as  Washington  county.  South- 
east of  Fond  du  Lac,  it  again  comes  out  to  the  margin  of  the  valley  above 
referred  to,  and  forms  the  white  cliffs  in  the  towns  of  Empire,  Eden, 
Byron  and  Oakfield.  In  this  region,  the  base  of  the  formation  is  thin 
bedded,  while  in  the  upper  portion,  the  beds  are  thicker.  South  of 
this,  the  formation  again  recedes  from  the  chain  of  ledges,  and,  at  a 
very  unfortunate  point  is  lost  beneath  the  drift  of  the  Kettle  Range. 
This  drift  moraine  crosses  the  strata  under  question  obliquely,  and  ef- 
fectually conceals  them  from  view  for  thirty  miles.  On  the  other  side 
of  the  range,  the  beds  at  Pewaukee  are  the  nearest  exposed  rock  east 
of  the  Mayville  beds. 

The  upper  strata  at  this  point  are  very  similar  to  the  Byron  beds 
in  color,  texture  and  composition,  but  in  fossils,  they  are  closely  rela- 
ted to  the  Racine  limestone,  while  the  Byron  beds  contain  but  few 
remains  of  any  kind,  and  are  separated  from  the  Racine  by  the  Coral 
beds,  containing  an  abundance  of  fossils,  less  closely  related  to  the 


NIAGARA  LIMESTONE. 

Racine  fauna  than  those,  of  the  Pewaukee  beds,  so  that  there  is  here 
presented  a  novel  and  interesting  question  of  equivalency,  that  will 
be  more  fully  appreciated  when  all  the  facts  are  before  us. 

The  strata  under  consideration  are  designated  Byron  beds  in  this 
report,  only  so  far  south  as  they  maintain  their  distinctive  character. 
They  have  been  regarded  by  some  geologists  as  the  equivalents,  in 
part,  of  the  Clinton  strata  of  Xew  York.  In  reference  to  this  ques- 
tion, the  attention  of  geologists  is  called  to  the  fauna  of  the  Mayville 
beds,  which  lie  between  these  and  the  Clinton  iron  ore  beds,  which 
shows  that  there  is  no  good  reason  for  separating  these  from  the  Ni- 
agara group. 

Economic  Considerations.  The  purity  of  the  rock  of  the  Byron 
beds  admirably  fits  it  for  the  manufacture  of  lime.  It  makes  a  strong 
and  white  article,  that  sustains  an  excellent  reputation.  In  selecting 
for  this  purpose,  the  granular  variety  is  generally  to  be  preferred, 
from  its  superior  purity,  and  because  its  somewhat  porous  nature  al- 
lows the  carbonic  gas  that  is  discharged  in  the  burning  to  escape  read- 
ily, thus  facilitating  an  easy  and  complete  calcination. 

In  the  towns  of  Oakfield  and  Byron,  kilns  have  been  established, 
that  manufacture  an  excellent  lime,  some  of  which  is  shipped  to  the 
Chicago  market.  To  the  northward,  where  the  formation  is  so  abun- 
dantly displayed,  it  is  but  little  burned,  as  the  local  demand  is  as  }-et 
small,  and  shipment  by  water  is  attended  \vith  risk. 

The  thicker  beds  furnish  an  excellent  building  stone,  either  rough 
dressed,  for  ordinary  masonry,  or  cut,  for  the  finer  classes  of  work. 
In  some  instances  a  color  as  white  as  statuary  marble  ma'y  be  ob- 
tained. 

In  the  town  of  Brillion,  and  less  notably  at  some  other  localities, 
the  strata  are  beautifully  mottled  and  banded  with  pink,  producing 
a  handsome  ornamental  stone.  It  is  fine  grained  and  close  textured, 
though  not  entirely  free  from  minute  pores,  and  possesses  sufficient 
hardness  to  be  capable  of  taking  a  fair  polish.  It  will  not  take  rank  as 
a  high  grade  of  marble,  but  should  find  a  place  as  an  ornamental  stone. 

As  considerable  sums  have  been  expended  on  this  series  of  lime- 
stones, in  search  of  marble,  it  may  be  well  to  remark  here  that  this  is 
an  undisturbed  sedimentary  formation,  lying  very  much  as  it  did 
when  deposited  by  the  ocean,  and,  while  it  has  crystalized  to  a  large 
degree,  there  is  no  evidence  that  it  has  undergone  any  unusual  degree 
of  heat  or  pressure,  and  there  is  no  reason  to  expect  that  any  portion 
of  it  will  present  that  indurated  and  perfectly  crystallized  character 
that  is  shown  by  metamorphic  rocks,  to  which  class  the  better  grade 
of  marble  belongs. 


348  GEOLOGY  OF  EASTERN  WISCONSIN. 

The  thinner  beds  of  this  formation  furnish  an  excellent  flagging. 
The  compactness  and  fine  grain  of  some  layers  fit  them  for  litho- 
graphic purposes,  but  they  are  apt  to  be  marred  by  occasional  small 
cavities  or  other  flaws. 

Transition  Beds.  Above  the  Byron  beds,  as  they  are  developed 
in  the  Green  Bay  peninsula,  there  lies  a  series  of  alternating,  coarse 
and  fine  grained  strata,  that  are  transitionary  in  character,  and  mark 
the  passage  from  the  fine  textured  Byron  beds  to  the  coarse  textured 
Coral  beds  above.  They  may  be  briefly  described  as  follows,  in 
descending  order: 

Beginning  at  the  base  of  the  Lower  Coral  beds,  there  occurs  first,  a 
hard,  tough,  conglorneritic  dolomite,  of  bluish  color,  mottled  with 
lighter. hues,  which  weathers  into  creases,  rather  than  pits.  It  has  a 
close,  but  uneven  texture,  and  contains  somfe  argillaceous  partings, 
and  a  few  cavities.  ISTo  fossils  were  seen  except  in  the  upper  layer, 
and  here  only  one,  not  observed  elsewhere.  This  consists  of  mi- 
nute, vertical,  cylindrical  canals,  somewhat  regularly  interspersed 
through  the  rock,  but  separated  from  each  other  by  several  times  their 
own  diameter.  The  general  appearance  is  similar  to  that  which 
would  be  given  if  a  small,  distant-tubed  Syringopora  were  to  be  en- 
tirely removed  by  solution,  leaving  only  its  external  cast  in  the  rock. 
It  seemed  to  be  confined  to  a  single  layer,  which  was  traced  2,000  feet, 
for  the  purpose  of  securing  the  dip,  which  was  found  at  this  point  — 
southwest  shore  of  Sturgeon  Bay  —  to  be  nearly  80  feet  per  mile, 
southwestward. 

Below  this  portion,  the  rock  is  uniform  in  texture,  close,  compact, 
fine  grained,  regularly  bedded,  smooth  on  the  weathered  exterior, 
even  in  fracture,  and  is  of  grayish  or  white  color.  No  fossils  were 
observed  in  this  portion. 

Below  this,  there  are  thick,  heavy,  granular  beds  of  coarse,  crystal- 
line texture,  and  irregular  hardness,  in  general,  quite  similar  to  the 
Lower  Coral  beds  in  lithological  characters,  but  containing  few  or 
no  fossils.  The  observed  thickness  of  these,  taken  together,  is  about 
30  feet. 

Below  this,  there  is  more  or  less  of  alternation  between  the  thin 
bedded,  compact  rock,  that  characterizes  the  Byron  beds  below,  and 
the  thick- bedded,  coarse-grained  rocks  that  represent  the  formations 
above.  The  conglomeritic  layer  is  the  only  one  that  is  not,  in  its  na- 
ture, allied  either  to  the  Lower  Coral  beds  above,  or  to  the  Byron 
beds  below. 


NIAGARA  LIMESTONE.  349 

LOWER   CORAL    BEDS. 

A  considerable  portion  of  the  transition  beds  just  described  are  to 
be  regarded  as  belonging  to  this  division.  The  rock  of  this  forma- 
tion is  a  rough,  heavy-bedded  dolomite,  not  unlike  the  Majville  beds, 
The  layers  are  sometimes  very  massive,  12  to  15  feet  intervening  be- 
tween distinct  bedding  joints.  In  one  case,  a  brecciated  reef -like  out- 
lier, 18  feet  in  height,  showed  no  bedding  lines.  This  massive  struc- 
ture is  an  occasional  feature  of  this  formation. 

In  texture,  the  rock  is  coarse,  crystalline,  granular,  and  usually  rath- 
er soft.  Occasional  layers  are  marked  by  argillaceous  seams  and  par- 
tings, and  by  bands  or  scattered  nodules  of  chert  or  flint,  or  by 
silicified  fossils.  The  softer  portions  usually  contain  frequent  cavi- 
ties, doubtless  formed  by  the  removal  of  fossils.  These,  together 
with  the  irregular  hardness  of  the  rock,  give  to  the  weathered  outliers 
a  very  rough,  craggy,  pitted  exterior.  The  prevailing  color  is  gray, 
verging  toward  blue,  white,  and  yellow,  at  times  occasionally  en- 
livened by  markings  of  red,  pink,  and  purple. 

Much  of  the  rock  is  a  nearly  pure  dolomite,  admirably  adapted  to 
the  manufacture  of  lime.  Some  portions  are,  however,  quite  silicious 
or  argillaceous,  and  the  discrimination  recommended  in  reference  to 
the  Mayville  beds  is  to  be  observed  here;  indeed,  the  economic  re- 
marks made  with  reference  to  that  subdivision  are  generally  applica- 
ble here,  and  need  not  be  repeated. 

Organic  Remains.  These  are  abundant  and  consist  very  largely  of 
corals,  among  which  the  genus  Favosites  predominates.  Brachiopods 
are  next  in  abundance,  among  wrhich  Pentamerus  is  most  prevalent. 

The  following  table  shows  the  leading  species  and  local  distribution 
in  a  compact  form: 


350  GEOLOGY  OF  EASTERN  WISCONSIN. 

FOSSILS  OF  THE  LOWER  CORAL  BEDS  OF  THE  NIAGARA  GROUP. 


GENERA  AND  SPECIES. 

3-H 

C<f 

1 

Cooperstown. 

Cato  (Mendliks). 

d 
,,vj 

S£ 

EH 

1 
O 

Kewaskum. 

X 
CO 

O 
£ 

PETROSFONGIA 

* 

* 

* 

CORALS. 

* 

* 

* 

* 

F.     Niagarensis  

* 

* 

* 

* 

* 

* 

* 

Astrocenum  venustum  

# 

* 

Halysites  catenulatus    

* 

* 

* 

* 

* 

* 

,,^-Jfr  catenulatus  var.,  microporus,  n.  var  

* 

AJH"."*  catenulatus  var.,  niacroporus,  n.  var  

* 

* 

H.     agglomeratus  .  .   

* 

Diphyphyllum  csespitosum  

* 

* 

Syringopora  Dalmani  

* 

S.     und.  sp  

* 

L/tUystostylus  typicus,  n.  gen.  and  sp  

* 

Cyanthophyllum,  und.  sp  

* 

Amplexus,  und.  sp  

* 

Zaphrentis,  und.  sp  

* 

* 

if 

# 

Aulacophyllum,  und.  sp  

* 

Chonophyllum,  und.  sp  

* 

* 

BRACHIOPODA. 

Dinobolus  Conradi  

* 

Trimerella,  res.  T.  grandis  

* 

Meristina,  und.  sp  

* 

Pentamerus  bisulcatus  

# 

* 

P.    oblongus  

* 

* 

* 

* 

P.    ventricosus  .  

* 

* 

Stricklandinia  

* 

* 

* 

GASTEROPODA. 

Straparollina,  und.  sp  

* 

Trochonema,  und.  sp  

* 

Pleurotomaria,  n.  sp  

* 

P.    und.  sp.  

* 

* 

Murchisonia  Hercynia  

* 

Bucania  trigonostoma  

* 

CEPHALOPODA. 

Orthoceras  alienum  

# 

0.    und.  sp  

* 

* 

* 

Discosorus  conoideus  

* 

Cyrtoceras  

* 

^  ^Pferagmoceras  labiatum,  n.  sp.  

* 

CRUSTACEA. 

Illsenus,  und.  sp  

* 

NIAGARA  LIMESTONE.  351 

It  is  difficult  to  state  definitely  the  thickness  of  this  subdivision, 
for,  as  already  seen,  its  lower  limit  is  not  well  defined,  and  it  is  equally 
difficult  to  fix  precisely  its  upper  boundary. 

The  greatest  thickness,  directly  observed,  was  48  feet,  but  this  does 
not  include  any  of  the  transitional  beds,  and  probably  not  all  others, 
as  the  section  was  incomplete.  If  we  include  that  portion  of  the  beds 
of  passage  below  and  above,  which  is  most  nearly  allied  to  this  divis- 
ion, the  maximum  thickness  will  be  about  70  feet. 

This  formation  is  very  closely  related  to  the  Upper  Coral  beds,  and 
the  distinction  between  the  two  is  less  marked  than  that  between  the 
other  subdivisions  of  this  group.  It  will  therefore  be  a  matter  of  con- 
venience to  describe  the  Upper  Coral  beds,  and  then  consider  their 
extent  and  local  developments  conjointly. 

UPPER   CORAL   BEDS. 

These  beds  directly  underlie  the  Racine  limestone  at  the  north,  and 
are  separated  from  them  by  a  sharp  line  of  division,  readily  distin- 
guishable wherever  observed. 

The  rock  is  a  rather  thin  bedded  dolomite,  generally  of  a  buff  color, 
as  seen  in  exposures,  but,  in  its  unweathered  condition,  often  grayish  or 
bluish.  It  is  usually  subcrystalline,  of  fine  grain,  compact,  and  hard, 
but  occasionally  earthy.  It  shows  a  tendency  to  split  into  irregular 
rudely  lenticular  flakes.  It  contains  much  silicious  material  in  the 
form  of  chert,  flint  or  silicified  fossils.  The  chert  is  usually  white, 
and  in  the  form  of  nodules,  but  graduates  into  dark,  translucent  vari- 
eties, which  pass  into  flint,  resembling  that  of  the  chalk  beds  of  Eng- 
land. The  carbonate  of  lime,  that  originally  constituted  the  material 
df  the  fossils,  has  been  replaced  in  many  cases  by  a  whitish,  chert- 
like  material,  and  in  others  by  translucent  and  transparent  forms  of 
cryptocrystalline  silica,  while  the  cavities  are  drusy  with  quartz. 
Silicified  fossils  are  more  common  than  the  unchanged  form,  and  on 
weathering,  these  project  from  the  surface,  giving  the  rock  a  very 
roueh,  harsh  exterior.  The  stone  is  of  little  value  for  construction  or 

O      " 

lime.     Some  layers  make  a  tolerable  flag. 

.  Organic  remains  are  exceedingly  abundant  in  this  formation,  among 
which  corals  mostly  predominate.  About  thirty  species  were  collect- 
ed, and  many  of  these  occur  in  great  number.  The  state  of  preserva- 
tion is  often  very  fine,  owing  to  silicification.  The  more  important 
localities  are  tabulated  below,  and  a  full  list  of  species  and  their  range 
will  be  found  in  the  general  table  of  fossils  of  the  Niagara  group. 


352 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  UPPER  CORAL  BEDS  OF  THE  NIAGARA  GROUP. 


GEXERA  AND  SPECIES. 

& 

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Scarboro  Creek,  T.  24 
R.  24,  S.  30. 

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Forrestville,  S.  17. 

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PLANTS. 

* 

PETROSPONGIA. 

Stromatopora  concentrica  

* 

* 

* 

* 

* 

* 

* 

* 
* 
* 
* 
* 

* 
* 

CORALS. 

* 

* 

* 

* 

* 

* 
* 
* 

P     Niagrarensis  •    

* 

* 

* 

F.    favosus,var.with  larger  cells 

* 
* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 
* 
* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

*'J 

* 

Thecia,  unrl.  sp.  with  small  cells 

* 

* 

* 

* 
* 

* 

Cladopora  reticulata  

* 
* 

* 

* 

* 

* 

* 

* 

* 
* 

.... 

Cyatbophylluni   und    sp  

* 

* 

Zaphrentis  sp.  res.  Z.  gigantea 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 

Aulacopliyllum  und..  sp  

* 

* 

* 

*v 

* 

Chonophylluin   und  sp  

* 

* 

* 

* 

* 

* 

Cystiphyliuin  Amencanum  .... 

* 

* 

* 
* 

* 

* 
* 

* 

S     n  sp    

* 

* 

* 

* 

Ccenites  lunatus  .  * 

* 

NIAGARA  LIMESTOXE. 


353 


FOSSILS  OP  THE  UPPER  CORAL  BEDS  OF  THE  NIAG_*RA  GROLT —  continued. 


GENERA  AND  SPECIES. 

tH 

a1 

W 
£ 

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CM 

02' 

3 

ctf 
0 

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Cato  Falls. 

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02' 

1 

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1 

00 
| 

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Kewaunee,  S.  14. 

Scarboro  Creek,  T.  24 
R.  24,  S.  30. 

od 

CM 

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Forrestville,  S.  17. 

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£» 

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,«OQ 

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cc 

Bailey's  Harbor. 

BRACHIOPODA. 

* 

* 

* 

Atrypa  reticularis  

* 

* 

* 

* 

* 

*? 

* 

* 

* 

P     n  sp    .           ... 

* 

Stricklandinia  n  sp  .  .         ... 

* 

* 

* 

GASTEROPODA. 

* 

CEPHALOPODA. 

Orthoceras  uncl  sp  

* 

* 

CRUSTACEA. 

* 

*? 

INCERTA  8EDES. 

H  uremia  annulata  

* 

* 

The  greatest  thickness  of  this  formation  actually  observed  is  75 
feet.  Its  maximum  thickness  is  estimated  at  90  feet. 

Distribution.  Beginning  at  the  north,  we  find  the  central,  and,  to 
a  great  extent,  the  eastern  portion  of  the  Green  Bay  peninsula  occu- 
pied by  the  Coral  beds,  the  lower  division,  of  course,  lying  to  the 
westward.  Extending  southward,  they  constitute  an  irregular  belt, 
occupying  a  median  position  on  the  Lake  Michigan  slope,  and  ceasing 
to  be  traceable  as  distinct  subdivisions  in  the  southern  portion  of 
Fond  du  Lac  county. 

Local  Details.  Near  the  eastern  entrance  of  Porte  de  Morts,  the  coral  beds  pre- 
sent themselves  in  vertical  cliffs,  facing  the  lake.  The  exposure  belongs  chiefly  to  the 
upper  division,  and  presents,  in  certain  portions,  more  than  the  usual  amount  of  cherty 
material.  In  general,  the  beds  are  highly  fossiliferous.  Silicified  specimens  of  Penta- 
merus  oblonyus,  of  rare  beauty,  are  occasionally  met  with. 

At  Bailey's  Harbor,  the  Upper  Coral  beds  are  exposed  in  nearly  their  entire  thick- 
Wis.  SUH.— 23 


354  GEOLOGY  OF  EASTERN  WISCONSIN. 

ness,  constituting  three  ten-aces,  rising  in  succession  from  the  lake  shore.  The  ledges 
here  are  extremely  fossiliferous,  and  this  locality  is  already  known  in  the  literature  of 
the  science.  The  uppermost  ledge  is  capped  by  a  few  layers  of  the  Racine  limestone. 
South  of  Jacksonport,  along  the  lake  shore,  the  Upper  Coral  limestone  is  again  ex- 
posed, presenting  a  thickness  of  twenty  feet,  with  its  usual  characteristics  and  abundance 
of  fossils. 

In  the  vicinity  of  Sturgeon  Bay,  several  exposures,  both  of  the  Upper  and  Lower  beds, 
occur.  In  Sec.  9,  there  are  several  slight  outcrops  of  the  upper  strata,  which  are  here, 
as  usual,  quite  cherty  and  contain  an  abundance  of  silicified  fossils,  among  which  the 
coralline  forms  predominate.  In  Sec.  5,  near  the  village  of  Sturgeon  Bay,  the  upper 
portion  of  the  Coral  beds  have  a  slight  exposure,  overlaid  by  a  few  of  the  Racine  beds. 
The  junction  between  the  two  is  here  sharp  and  well  defined,  the  uppermost  layers  of 
the  Coral  beds  being  highly  fossiliferous,  a  fact  which  does  not  seem  to  be  universally 
true,  as  at  several  other  points  the  beds  lying  immediately  beneath  the  Racine  lime- 
stone are  comparatively  free  from  fossils.  North  of  the  village,  near  the  mill,  the  Lower 
Coral  beds  are  shown  imperfectly,  but  in  considerable  thickness.  Still  farther  north, 
along  the  cliffs  facing  the  bay,  at  various  points,  partial  sections  of  the  same  beds  are 
exposed.  On  the  opposite  side  of  the  bay  are  numerous  partial  exposures  of  the  Lower 
Coral  beds  overlying  the  Byron  beds.  Following  the  outcrops  of  the  formation  south- 
ward, Greening's  ledge,  in  the  town  of  Forrestville  (S.  W.  qr.  Sec.  17),  is  worthy  of 
note  for  the  remarkable  abundance  of  fossils  which  it  presents.  Passing  by  several 
minor  exposures,  we  find,  on  Scarboro  creek,  in  the  town  of  Casco,  and  in  Sec.  28  of  the 
town  of  Pierce  (T.  24,  R.  24),  the  Upper  Coral  strata  presenting  their  usual  thin,  irreg- 
ular, cherty  outcrops,  and  characterized  by  an  unusual  abundance  of  well  preserved 
silicified  fossils.  The  latter  locality  is  remarkable  for  the  great  number  of  Favositoid 
corals,  large  masses  of  Syringopora,  and  frequent  specimens  of  Stronibodes,  in  associa- 
tion with  an  abundance  of  the  more  usual  forms.  In  Sec.  14,  in  the  town  of  Kewannee, 
at  the  mill  of  Mr.  Stramsky,  the  uppermost  layers  of  the  Coral  beds  are  found  immedi- 
underlying  the  Racine  limestone.  They  are  here  more  homogeneous  and  less  cherty 
than  at  most  localities  to  the  northward,  and  much  less  fossiliferous  than  the  corres- 
ponding beds  at  Sturgeon  Bay,  only  five  or  six  species  being  observed.  In  the  valley  of 
West  Twin  river,  several  notable  exposures  of  this  formation  occur.  In  Sec.  28,  town  of 
Gibson,  a  vertical  thickness  of  about  forty  feet,  belonging  to  the  lower  division,  is  ex- 
posed. The  upper  portion  of  the  ledge  consists  of  very  heavy  beds  of  coarse,  rather  soft 
dolomite,  characterized  by  fine  specimens  of  coral.  The  lower  portion  of  the  ledge  con- 
sists of  a  harder  and  more  compact  rock  of  finer  texture,  very  prolific  in  Pentamerus. 
In  the  vicinity  of  the  junction  of  Mud  creek  with  the  West  Twin  river,  particularly  in 
Sec.  13,  Cooperstown,  ledges  that  appear  to  represent  the  transition  from  the  Lower 
Coral  beds  to  the  Byron  beds  find  ample  exposure.  The  following  section  is  observed 
near  the  center  of'  Sec.  13. 

1.  At  the  top,  a  broken,  grayish  white  dolomite,  mottled  with  pinkish 

red,  of  porous,  rather  hard,  brittle,  crystalline  texture  and  uneven 
fracture,  in  beds  of  18,  11^,  15  and  13%  inches,  respectively.  The 
lower  layers  are  more  compact  than  those  above 4  ft.  10  in. 

2.  Harder  laminated  dolomite,  of  slightly  porous  texture,  gray,  lined 

with  pink 1  ft.    5^  in. 

3.  Similar  to  No.  1,  but  more  coarse  and  porous  in  texture,  and  rougher 

in  general  aspect 2  ft.    2Hn. 

4.  Similar  to  No.  2,  but  not  distinctly  laminated.     In  beds  of  7%,  12  and 

11  inches  respectively 2  ft.    62  in, 

5.  Rather  soft,  granular  dolomite,  of  sandy  appearance,  streaked  with 

white  and  yellow,  and  distinctly  blotched  with  copper  red 6    in. 


NIAGARA  LIMESTONE.  355 

6.  Rather  hard,  compact  dolomite,  mottled  with  purplish,  pink  and 

white,  containing  a  few  very  small  drusy  geodes.     Weathers  smooth,     1  ft.     6    in, 

7.  Coarsely  porous  dolomite,  of  uneven  texture,  prominently  mottled 

with  scarlet,  pink  and  purple,   and  containing  corals  and  drusy 

geodes.     Marked  with  stylolites 2  ft.    3    in. 

8.  Rather  hard,  firm,  laminated  dolomite,  rather  thin  bedded,  having  a 

bnttle,  uneven  fracture.     In  successive  beds  of  9^,  13,  9,  13,  and 

5%  inches 4  ft.     2i  in. 

9.  Very  fine  grained,  compact,  flint-like  dolomite,  of  smooth,  hard,  semi- 

conchoidal  fracture,  and  bluish  and  yellowish  gray  color.     In  beds 

of  11,  1%,  4:%,  5,  3%,  4%,  9,  6>4,  and  7  inches  respectively 4  ft.  lOf  in. 

10.  Compact,  but  more  granular  crystalline  than  the  above,  of  whitish 
gray  color.  In  beds  of  9>  6,  9,  8>£,  2%,  and  11  inches,  the  lowest 
of  which  is  banded  with  purple 3  ft.  10  in. 


Total 28ft. 


In  the  vicinity,  higher  and  more  fossiliferous  beds  find  limited  exposure.  In  Sec.  25 
of  this  town,  there  is  -a  peculiar  outlier  of  18%  feet  vertical  exposure,  presenting  no 
v>rell- defined  bedding.  The  rock  is  a  rather  hard,  coarsely  brecciated,  light  colored 
dolomite,  weathering  very  rough,  and  containing  few  fossils.  It  resembles  some  of  the 
brecciated  portions  of  the  Lower  Maguesian  limestone  previously  described,  but  more 
especially  the  reef  structure  of  the  Racine  limestone,  yet  to  be  considered. 

Passing  by  a  number  of  minor  outcrops  in  this  vicinity,  in  Sec.  5,  of  the  town  of  Cato^ 
is  a  notable  ledge  arising  to  the  height  of  46  feet,  which  consists  of  heavy,  irregularly 
bedded  dolomite,  of  coarsely  brecciated  structure  for  the  most  part,  but,  to  some  extent, 
coarsely  granular,  and  containing  abundant  cavities  of  various  sizes,  often  filled  with 
calcite,  many  of  which  are  evidently  the  result  of  the  entire  or  partial  removal  of  fossils. 
Corals  are  present  in  abundance.  In  the  N.  W.  ^  of  the  N.  W.  %  of  the  same  section 
is  an  isolated  ledge  of  somewhat  similar  character,  but  rather  more  thin-bedded  and 
compact,  and  differing  from  the  former  in  the  presence,  in  some  layers,  of  much  chert, 
in  which  fossils,  most  beautifully  silicified,  are  abundant,  Pentamerus  oblongus  beinj^ 
the  predominating  form.  In  Sec.  6  of  the  same  town,  on  the  farm  of  Mr.  J.  Mendlik, 
is  a  conspicuous  ledge,  consisting  of  very  heavy  bedded,  rough,  inegular  dolomite,  of 
varying  hardness,  usually  rather  soft,  brecciated  for  the  greater  part,  white  or  gray 
in  color,  and  variously  mottled  and  streaked  with  pink.  The  structure  is  very  irregular. 
The  rock  contains  many  corals,  especially  those  belonging  to  the  genus  Favosites,  and 
a  few  other  fossils. 

Another  noteworthy  ledge  occurs  near  the  middle  of  the  south  half  of  Sec.  36,  town  of 
Richland.  The  following  section,  in  descending  order,  was  noted  at  that  point: 

1.  Hard,  white,  compact,  somewhat  cherty  dolomite,  containing  occa- 

sional cavities,  and  showing  a  slight  tendency  to  separate  on  the 
weathered  surface  into  thin  beds 10  ft. 

2.  Hard,  grayish  white  dolomite  of  uneven  texture,  and  subcrystalline, 

irregular  fracture,  marked  by  numerous  argillaceous,  lamellar  part- 
ings, and  a  few  geodes.  Weathers  irregularly  into  deep  pits.  In 
layers  of  3  feet  4  inches,  2  feet  6  inches,  and  3  feet 8  ft.  10  in. 

3.  A  softer  and  more  granular  stratum,  containing  Cyathophylloid  corals, 

which  were  not  observed  in  the  upper  beds 3  ft.     2    in. 

4.  A  stratam  of  irregular,  grayish  white,  shaly  dolomite  of  uneven  tex- 

ture, which  weathers  into  rough  creases 4  ft. 


356  GEOLOGY  OF  EASTERN  WISCONSIN. 

5.  White,  rather  soft,  granular  crystalline  doiomite,  of  more  even  tex- 

ture than  the  above,  and  better  suited  for  cutting.   Weathers  smooth. 

In  layers  of  10  to  13  inches , 2  ft.  11    in. 

6.  Tnin,  regular  bedded,  white,  granular  crystalline,  rather  soft,  some- 

vrhat  shaly  dolomite,  in  layers  from  3  to  9  inches  in  thickness,  par- 
tially concealed 3  ft.     9    in. 

7.  Pure,  opaque  white,  saccharoidal  dolomite,  of  medium  hardness  and 

even  texture,  weathering  comparatively  smooth.     In  layers  of  13, 

16,  17,  36,  16,  and  10  inches,  which  occasionally  unite  or  subdivide.     9  ft. 

8.  Granular  crystalline  dolomite,  of  medium  hardness,  somewhat  un- 

even texture,  white  and  pale  orange  color,  mottled  and  mingled. 

Layers  not  always  well  defined 6  ft.     6    in. 


Total 48ft.    2    in. 


At  Cato  Palls,  on  the  Manitowoc  river,  thinner  and  more  homogeneous  beds,  belong- 
ing to  a  higher  horizon,  appear  in  undulating  stratification.  At  Clark's  mills,  two 
miles  below,  similar  thin  beds,  in  broken  ledges,  form  a  wall  along  the  bank  of  the  river, 
rising  from  10  to  15  feet  in  hight,  and  are  characterized  by  abundance  of  corals  of  the 
genus  Favosites.  Near  the  old  mill,  a  short  distance  below  Clark's  mills,  on  the  left 
hand  side  of  the  river,  occurs  a  slight  outcrop,  the  top  of  which  is  very  cherty,  and  con- 
tains silicified  fossils,  the  most  conspicuous  of  which  is  the  remarkable  Cyathophylloid 
coral,  Amplexus  fenestratus,  n.  sp.,  which  attains  a  foot  or  more  in  length,  and  two  or  three 
inches  in  diameter.  A  short  distance  down  the  river,  from  20  to  25  feet  of  impure,  brec- 
ciated  limestone  is  overlaid  by  about  12  feet  of  cherty  rock  containing  the  above  men- 
tioned coral,  the  whole,  from  its  hardness,  giving  rise  to  the  rapids.  It  is  worthy  of 
note  that  these  two  localities  are  the  only  ones  at  which  the  above  fossil  has  been  found. 
South  of  the  Manitowoc  river,  the  formation  is  overlaid  for  a  considerable  distance  with 
the  glacial  accumulations  of 'the  Kettle  Range,  and  effectually  concealed  from  observation. 

In  Sees.  2  and  11  of  the  town  of  Ashford,  Fond  du  Lac  county,  the  railroad  exca- 
vations again  bring  the  formation  to  our  notice.  In  the  former  section,  the  rock  is  a 
soft,  yellowish  dolomite  of  irregular  texture  and  bedding,  and  is  specially  interesting  for 
the  variety,  abundance  and  peculiarity  of  its  fauna,  as  will  be  seen  by  Deference  to  the 
table.  The  cut  in  Sec.  11  presents  a  rock  whose  lithological  characters  are  not  essen- 
tially different  from  the  preceding,  but  which  contains  a  very  great  abundance  of  Penta- 
merus  oblongus,  in  great  variety  of  size  and  form,  and  an  almost  entire  absence  of  the 
fossils  which  characterize  the  preceding  location.  At  the  village  of  Elmore,  in  the  same 
township,  a  quarry  exhibits  a  heavy  bedded  rock  of  much  more  firm  and  homogeneous 
texture,  the  sole,  but  abundant,  fossil  of  which  is  Pentamenis  oblongus,  in  unusually  largo 
and  fine  specimens. 

In  the  N.  W.  ^  of  Sec.  6,  in  the  town  of  Kewaskum,  at  Kuhn's  quarry,  is  a  porus, 
granular,  crystalline  dolomite,  containing  an  abundance  of  Favositoid  corals  and  Penta- 
tnerus  oblongus,  and  probably  represents  the  horizon  of  the  Lower  Coral  beds.  South- 
ward from  this  point,  the  formation  is  lost  under  the  Kettle  Range,  and  we  do  not  again 
rec  it,  or  what  may  be  supposed  to  be  its  equivalent,  until  we  reach  the  vicinity  of  Pe- 
waukee.  On  the  Sheboygan  river,  at  the  village  of  Roekville,  there  is  a  slight  expos- 
ure of  the  upper  portion  of  the  Upper  Coral  beds,  presenting  a  more  than  usually  dark 
gray  color,  with  more  or  less  of  chert,  and  containing  but  very  few  fossils.  The  drift 
in  the  vicinity,  however,  is  prolific  in  those  species  which  are  so  abundantly  present  far- 
ther to  the  north. 


NIAGARA  LIMESTONE.  357 

WAUKESIIA    BEDS. 

The  terra  Waukesha  limestone  was  selected  many  years  since  by 
Dr.  Lapham,  to  designate  the  thin  bedded  strata  that  occur  at  Wau- 
kesha,  and  their  equivalents  elsewhere.1  This  term  was  also  adopted 
by  Prof.  Hall,  in  the  report  of  1862.2  It  seems  therefore  desirable 
to  retain  a  name  that  has  already  become  fixed  in  the  literature  of  the 
subject,  although  we  shall  be  compelled  to  restrict  its  application,  and 
to  entertain,  to  some  extent,  different  views  as  to  its  relations. 

There  are  at  Waukesha  three  classes  of  limestone.  In  the  quarry 
near  the  college,  the  upper  fourteen  feet  consist  of  a  soft,  yellowish, 
coarse-textured  dolomite,  that  has  been  identified  with  unquestioned 
correctness,  as  the  equivalent  of  the  Racine  limestone.  This  reposes 
upon  regular,  even  beds  of  a  hard,  compact,  fine-textured,  crystalline 
dolomite,  of  gray  color  and  conchoidal  fracture.  It  is  characterized 
by  the  presence  of  much  chert  in  the  form  of  nodules,  distributed 
chiefly  in  layers,  coinciding  with  the  bedding  joints.  These  strata 
abound  in  Orthoceratites,  but  contain  few  other  fossils.  They  consti- 
tute the  type  of  the  Waukesha  beds.  The  transition  to  the  Racine 
beds  is  quite  abrupt,  but  does  not  correspond  to  a  bedding  joint. 
From  three  to  four  inches  of  the  base  of  a  thick  layer  are  of  compact 
rock,  like  that  below,  while  the  remainder  has  the  open  texture  and 
fossils  of  the  Racine  beds. 

Passing  by  several  intermediate  quarries,  for  the  moment,  we  find 
at  the  lime  kilns,  two  miles  above  Waukesha,  a  fine  display  of  the 
Racine  limestone  reposing  upon  similar  cherty  flags,  which  form  the 
sole  of  the  quarry.  The  transition  is  accomplished  in  a  manner  pre- 
cisely similar  to  that  above  described. 

In  the  road,  south  of  this  quarry,  the  porous  Racine  rock  appears, 
but  one  hundred  yards  beyond,  and  at  the  same  elevation,  occurs  a 
light  colored,  hard,  compact,  close-grained,  subcrystalline  dolomite, 
resembling  closely  the  Waukesha  flags,  except  that  chert  is  absent. 
A  few  rods  further,  a  quarry  has  been  opened,  exposing  these  strata 
more  satisfactorily.  In  addition  to  the  close  textured  rock,  there  are 
layers  of  mottled  blue  and  white  color,  and  irregular,  lumpy  struc- 
ture, such  as  are  associated  with  the  even-bedded  rock  in  the  vicinity 
of  the  Niagara  reefs  near  Milwaukee.  Several  openings  follow  at 
short  intervals,  including  the  main  quarry  of  Mr.  Hadfield,  all  of 
which  exhibit  the  same  character.  This  is  also  true  of  the  several 
quarries  on  the  opposite  side  of  the  Fox  river.  I  have  elsewhere  dem- 

1  See  Owens1  Geological  Survey  of  Wisconsin,  Iowa  and  Minnesota,  p.  455. 

2  Geology  of  Wisconsin,  1862,  pp.  56-64;  also  note  on  pp.  446-448. 


358  GEOLOGY  OF  EASTERN  WISCONSIN. 

onstrated  that  the  coarse,  open-textured  Racine  limestone  graduates 
horizontally  into  a  precisely  similar  compact  rock,  and  am  therefore 
inclined  to  consider  the  weight  of  evidence  as  favoring  the  conclu- 
sion that  such  is  the  case  here.  In  this  view,  the  flags  and  thicker 
even- bedded  rock,  on  either  side  of  the  Fox  river  above  Waukesha, 
would  be  regarded  as  belonging  to  the  Racine  beds,  being  the  strati- 
graphical  equivalents  of  the  coarse-grained  Racine  layers.  The  only 
undoubted  members  of  the  Waukesha  beds  are,  then,  the  cherty  flags 
near  the  college  and  at  the  kiln. 

Farther  up  the  stream,  in  Sec.  31,  Menomonee,  similar  cherty  flags 
make  their  appearance,  and  they  also  occur  in  the  drift  at  intermediate 
points. 

At  Pewaukee,  the  upper  strata  consist  of  a  white,  fine-grained,  but 
porous  crystalline  dolomite,  having  a  conchoidal  fracture.  In  this 
portion  occur  the  crinoids  Caryocrinus  ornatus,  Eucalyptocrinus 
craqsus,  E.  coslatus,  E.,  n.  sp.,  and  the  trilobites,  Illmnus  loxus  and 
/.  pterocephalus,  n.  sp.,  in  association  with  several  Orthoceratites  and 
other  fossils,  thus  manifesting  a  noticeable  affinity  to  the  Racine 
fauna. 

The  lower  layers  at  this  point  are  more  argillaceous  and  silicious, 
and  of  more  irregular  texture,  with  patches  of  cherty  material.  Ha- 
lysites,  Favosites  and  Pentamerus  occur  in  these  beds.  In  one  por- 
tion of  Mr.  Pel  ton's  quarry  a  layer  is  almost  entirely  composed  of 
a  large  Pentamerus  oblongus,  imbedded  in  white  dolomitic  material, 
forming  a  rather  heavy  bedded  rock  of  uneven  texture.  It  lies  near 
the  base  of  the  quarry,  but  from  its  situation  and  the  undulating  na- 
ture of  the  strata,  its  relation  to  the  impure  layers  above  mentioned 
are  not  apparent.  It  is  quite  possible  that,  as  suggested  by  Prof. 
Whitfield  on  paleontological  evidence,  the  upper  portion  belongs  to 
the  Racine,  and  the  lower  to  the  Waukesha  horizon.  The  list  of  fos- 
sils, collected  at  this  ponit, is  as  follows:  Stromatopora  concentrica, 
Favosites  favosus,  Astrocerium  venustum,  Holy  sites  catenulatus,  Za- 
phrentis,  Omphyma,  Caryocrinus  ornatus,  Eucalyptocrinus  crassus, 
E.  ccelatus,  E.,  n.  sp.,  Streptorhynchus  subplanum,  Strophomena 
rhomboidalis,  Spirifera  nobilis,  Meristina  Maria,  Atrypa  reticularis, 
Pentamerus  oolongus^  P.  ventricosus,  Orthoceras  annulabum,  0. 
alienum,  O.  medulare,  0.  crebescens,  Oyroceras  Hercules,  Gomphoc- 
eras  nautilus,  n.  sp.,  Illcenus  loxus,  and  /.  pterocephalus,  n.  sp. 

An  interesting  feature  of  this  locality  is  a  mound  of  rock  lying  a 
short  distance  west  of  the  main  quarries  which  rises  ten  or  twelve 
feet  above  its  base,  and  has  a  diameter  of  only  a  few  rods.  It  con- 
sists of  very  irregular  beds,  coalescing  promiscuously  with  each  other 


NIAGARA  LIMESTONE.  359 

and  dipping  irregularly  in  all  directions.  The  rock  is,  for  the  most 
part,  hard,  compact,  white,  and,  in  some  portions,  cherty,  and  con- 
tains a  few  Brachiopods.  It  evidently  owes  its  origin  to  irregulari- 
ties of  deposition  and  not  to  upheaval. 

Johnson's  quarry  in  the  town  of  Genesee,  presents  a  vertical 
exposure  of  more  than  25  feet,  of  a  beautiful  white,  fine-grained 
dolomite,  in  beds  of  20  inches  thickness  and  less,  having  an  eastward 
dip  of  one  foot  in  sixty.  Near  the  base  a  layer  possesses  the  mottled 
color  and  uneven  texture  above  decribed.  Fossils  are  rare  in  this 
location.  A  few  rods  distant  on  the  opposite  side  of  the  road,  a 
quarry  displays  very  similar  beds,  but  they  are  rather  more  por- 
ous in  general  and  abound  in  chert  in  certain  layers  which  is 
rare  or  absent  at  the  former  locality.  They  are  also  more  fos- 
silferous,  though  not  abundantly  so.  The  following  species  were 
collected:  Of  Crinoids,  Caryocrinus  ornatus,  Eucalyptocrinus 
crassus,  and  E.  co&latus;  of  Brachiopods,  Orthis  flabellula^  Spirifera 
plicatella,  Atrypa  reticularis,  Rhynchonella  Indianensis ;  the  Gas- 
teropod,  Platyostoma  Niagarense ;  of  Gephalopods,  Orthoceras  an- 
nulatum,  0.  alienum,  0.  columnare,  0.  medulare,  0.  n.  sp.,  Oyr- 
toceras  Orcas,  Gyroceras  Hercules,  and  the  Trilobite,  Illcenus  ioxus ;  a 
a  fauna  very  closely  resembling  that  of  Pewaukee. 

In  the  rise  of  the  hill,  immediately  to  the  east,  the  typical,  yellow, 
coarse-grained  Racine  limestone  appears,  as  it  also  does  in  the  adja- 
cent ridge  on  the  south.  It  is  probable  that  many  of  the  prominent 
hills  in  this  region  contain  a  core  of  Racine  limestone;  though  deeply 
overlaid  by  the  almost  universally  prevalent  drift. 

Closely  allied  strata  occur  at  Castleman's  quarry,  in  the  town  of 
East  Troy,  but  no  distinct  fossils  were  found.  The  locality  is  widely 
separated  by  deep  drift  from  all  other  outcrops: 

Returning  to  the  vicinity  of  the  typical  locality  in  Waukesha  coun- 
ty, we  find  in  Sec.  3-4,  of  the  town  of  Lisbon,  a  formation  that  may  be 
said  to  be  identical  in  character  with  the  upper  strata  at  Pewaukee. 
To  the  east  and  northeast,  in  that  and  the  adjoining  town,  are  numer- 
ous openings  upon  white,  or  light  colored,  fine-grained,  even  bedded 
dolomite,  with  few  or  no  fossils,  which  renders  their  place  in  the 
series  somewhat  doubtful. 

As  the  horizon  of  the  Waukesha  beds  is  traced  northward,  it  plun- 
ges beneath  the  deep  drift  of  the  Kettle  Range,  and  on  emerging  be- 
yond, the  Byron  beds  and  the  Upper  and  Lower  Coral  beds  are  found 
to  occupy  the  space  between  the  Racine  beds  above  and  the  Mayville 
below.  The  cherty  flags  at  "Waukesha  most  closely  resemble  the  up- 
per portion  of  the  Upper  Coral  beds,  which  occupy  the  same  strati- 


360  GEOLOGY  OF  EASTERN  WISCONSIN. 

graphical  position  beneath  the  Racine  strata,  but  nowhere  in  the 
southern  counties  is  there  manifested  that  abundance  and  variety  of 
coralline  forms  that  distinguish  the  formation  to  the  northward. 
The  Pentamerus  beds  at  Pewaukee  bear  a  closer  alliance  to  certain 
members  of  the  Lower  Coral  beds  than  to  any  other  member  of  the 
northern  Niagara  series,  while  the  white,  compact,  chertless  beds  bear 
so  striking  a  lithological  resemblance  to  the  Byron  beds,  that  they 
have  been  sometimes  regarded  as  equivalents.  But  to  satisfy  all  these 
affinities  would  be  to  impose  incredible,  if  not  impossiblej  demands  up- 
on the  stratigraphical  relations  of  the  southern  members,  besides,  the 
affinities  are  not  by  any  means  unequivocal. 

The  facts  seern  to  be  that  in  this  case,  as  with  the  lower  formations, 
the  deposits  in  the  southern  counties  differ  from  the  corresponding 
ones  in  the  northern  counties,  and  that  the  Waukesha  group  of  strata 
is  the  equivalent  of  the  three  more  ponderous  northern  members  that 
lie,  like  it,  between  the  Mayville  and  Racine  horizons. 

On  Plate  X  of  the  accompanying  atlas,  white  lines  have  been  used 
to  designate,  in  a  general  way,  the  surface  area  of  each  of  the  sub- 
divisions of  the  Niagara  group.  Within  the  spaces  included  be- 
tween these  lines  are  often  limited  —  and  occasionally  considerable  — 
areas  of  a  higher  member  occupying  the  summit  of  prominences,  or. 
of  a  lower  member,  reached  by  deep  erosion.  Within  the  general 
area  of  the  Waukesha  beds,  patches  of  Racine  limestone  occur,  as  al- 
ready cited  in  Genesee.  The  white  lines  for  this  subdivision  were 
drawn  so  as  to  include  all  of  the  known  cherty  flags  belonging  to  this 
horizon. 

KACINE   BEDS. 

Overlying  the  Waukesha  beds  at  the  south,  and  the  Upper  Coral 
beds  at  the  north,  is  a  magnesian  limestone  to  which  the  term  Racine 
has  been  applied,  from  its  important  development  at  that  point.1  It 
has  an  extent  of  about  200  miles,  reaching  from  Illinois  to  near  the 
extremity  of  the  Green  Bay  peninsula,  and  attains  a  surface  width  of 
thirty  miles.  In  its  southern  portion,  where  it  rests  upon  the  Wau- 
kesha limestone,  it  consists  of  reef-like  masses  of  conglomeritic  rock, 
which,  on  the  denuded  surface,  appear  as  mounds  or  ridges,  and  which 
graduate  into  various  kinds  of  porous,  granular,  irregularly  bedded 
rock,  or  into  fine  grained,  compact,  even-bedded  strata,  the  whole  con- 
stituting a  formation  of  exceedingly  irregular  structure.  In  its 
northern  portion,  where  it  reposes  on  the  Upper  Coral  beds,  it  pos- 
sesses a  much  more  uniform  character.  On  account  of  these  pecu- 

1  Report  of  1862,  p.  67. 


NIAGARA  LIMESTONE.  361 

liarities,  it  is  thought  best  to  depart  from  our  usual  order  of  descrip- 
tion, so  far  as  to  consider,  first,  the  local  peculiarities  of  the  formation, 
after  which  we  may,  with  more  satisfaction,  indulge  in  generalizations 
and  draw  conclusions. 

Local  details.  At  Racine,  whence  the  formation  takes  its  name,  as  exposed  at  the 
rapids  of  Boot  river,  it  is  a  blue,  gray  or  buff,  brittle  dolomite,  having  a  somewhat  glassy 
fracture,  subcrystalline  structure  in  part,  and  earthy  in  part,  and  contains  many  geodic 
cavities,  filled  with  calcite  and  pyrite,  and  sometimes  mammillary  deposits.  Its  texture 
is  uneven,  being  sometimes  granular  and  again  brecciated,  usually  coarse  and  porous, 
but  sometimes  fine  and  compact.  It  is  frequently  stained  with  iron  oxide,  and,  in  places, 
is  quite  pyritif  erous,  especially  in  the  fissures.  The  bedding  is  also  irregular,  but  usually 
rather  heavy,  ranging  from  five  feet  downwards.  In  the  south  quarry  at  this  point,  be- 
longing to  Mr.  florlick,  there  is  a  small  mound  of  highly  porous  blue  rock,  without  vis- 
ible bedding,  full  of  fossils,  from  which  it  doubtless  had  its  origin,  after  the  manner  of 
reef  formation.  It  is  surrounded  on  all  sides  by  bedded  rock.  The  dip  at  this  point  is 
varying  in  amount  and  direction,  as  shown  by  the  following  record  of  observations  in 
different  parts  of  the  three  quarries  near  the  rapids  : 

EAST   QUARRY. 

Dip  8°.    Direction  ...........................................  N.  47°  W. 

Dip?0.  "      ...........................................  N.40°W. 

Dip  1°.  "      ............................................  N.  55°  W. 

Dip3^'-        "      ............................................  W.45°    S. 

WEST   QUARRY. 

Dip  5°.     Direction  ............................................  N.  65°  W. 

Dip  \yz°.     "    ................  ............................  N.  11°  w. 

Dip2°.  "      ......................  .  .....................  N.30°W. 

Dipl°.  "      ............................................  N.63°W. 

NORTH  QUARRY,   WEST   SIDE. 


Dip  0° 

Dip  1° 

ii 

S  80°   E 

NORTH   QUARRY,   EAST   SIDE. 

Dip  0° 

Dirt  1°. 

(I 

.  N.  30°  E. 

It  is  understood,  of  course,  that  these  measurements  were  made  in  different  parts  of 
the  quarries,  and  on  different  layers,  and  they  doubtless  do  not  in  all  cases  represent  tho 
true  dip;  i.  e.,  the  maximum  inclination,  as  the  exposure  often  did  not  render  the 
demonstration  of  this  possible.  But  the  general  fact  of  irregularity  is  sufficienty  shown, 
and  it  is  to  be  noticed  that  the  average  dip  is  to  the  N.  W.,  a  direction  opposite  to  the 
general  dip  of  the  formation. 

Fossils  are  very  abundant,  in  the  form  of  imperfect  casts.  At  Vaughn's  quarry,  less 
than  two  miles  distant,  the  first  six  01  eight  feet,  as  it  lies  in  the  beds,  is  deep  yellow  in 
color,  verging  to  orange  and  red  on  the  one  hand,  and  to  pale  buff  on  the  other.  Below 
this  the  color  varies  from  ashy-gray  to  grayish-blue.  The  upper  layers  are  apparently 
thinner  bedded  than  those  below,  though  this  is  probably  only  the  effect  of  the  elements. 
The  lower  layers  are  heavier,  but  do  not  often  exceed  a  foot  in  thickness.  The  beds  are 
but  obscurely  defined,  so  that  it  is  difficult  to  trace  a  given  one  for  any  considerable  dis- 
tance, or  to  ascertain  the  dip  with  any  precision.  There  is  an  almost  entire  absence  of 


362  GEOLOGY  OF  EASTERN  WISCONSIN. 

slialy  partings  or  laminae  of  clay,  so  that  the  dripstone  arc  comparatively  free  from  thcj 
marly  or  clayey  matter  common  in  quarries.  This  is  only  true  of  the  lower  layers  that 
have  not  been  affected  by  inwashing  from  above,  and  by  the  immediate  action  of  the 
surface  elements. 

The  vertical  joints  are  prominent,  and  in  soma  portions  frequent,  and  are  usually 
smooth,  and  coated  with  calcareous  and  pyritiferous  deposits. 

The  rock  is  porous  and  geodif erous ;  the  former  condition  being  largely  due  to  crin- 
oidal  remains  imperfectly  preserved,  and  the  latter  perhaps  in  part  to  the  same  cause, 
also,  the  portion  removed  being  the  calyx.  The  material  filling  the  geodes  is  chiefly  cal- 
cite  and  pyrite,  both  of  which  appear  in  abundant  and  beautiful  forms.  The  pyrite 
takes  the  tabular  form  of  crystallization  to  a  large  extent,  and  the  calcite  seems  to  pre- 
fer the  form  known  as  dog-tooth  spar.  Crystals  of  this  an  inch  or  more  in  length  are  not 
uncommon. 

The  rock  is  quite  brittle  and  sonorous,  and  presents  a  saccharoidal  appearance  on  the 
freshly  fractured  surface  of  the  unweathered  layers.  A  bluish  green,  argillaceous  ma- 
terial is  found  in  obscure,  irregular  partings. 

In  fossils,  it  is  far  less  prolific  than  the  rock  at  the  Rapids. 

At  the  quarries  belonging  to  Mr.  Trimbone,  in  the  town  of  Greenfield,  Milwaukee 
county,  the  rock  is  chiefly  a  light  buff,  porous,  granular,  brittle  dolomite,  rather  soft, 
and  in  some  cases  almost  friable,  and  at  points  disintegrating  to  a  calcareous  sand.  A 
little  calcite  in  crystals,  but  no  pyrite  was  seen.  The  fracture  is  rough,  but  usually 
along  the  line  indicated  by  the  application  of  the  force,  the  manner  in  which  the  force  is 
applied,  rather  than  the  nature  of  the  rock,  determining  the  line  of  fracture. 

But  in  the  southeastern  quarry,  the  rock  differs  considerably  from  the  rest,  being1 
harder,  finer,  more  compact,  less  brittle,  and  bluer. 

In  general,  the  beds  are  from  1%  to  3  feet  in  thickness,  but  readily  split  into  thinner 
layers.  The  beds,  though  in  general  regular  and  somewhat  uniform,  not  unfrequently 
thicken,  and  curve,  or  undulate.  Indeed,  the  last  feature  seems  to  be  a  common  char- 
acteristic when  any  considerable  area  is  considered,  so  much  so  as  to  render  any  attempt 
to  get  the  general  dip,  by  local  observations,  utterly  futile.  These  undulations  are  not 
regular,  nor  do  they  present  a  system,  as  though  due  to  some  common  cause,  as  contrac- 
tion or  upheaval,  but  are  in  a  sense  inharmonious  with  each  other.  The  phenomenon 
arises,  doubtless,  in  irregularities  of  deposition,  and  not  in  subsequent  folding  or  other 
disturbance.  A  little  careful  study  is  decisive  on  this  point.  One  of  the  clearest  illus- 
trations of  this  is  to  be  found  in  the  southeastern  quarry,  where  the  lower  bedding  joints 
can  be  traced  in  a  straight  line  beneath  the  apparent  folding.  The  next  ones  are  lost  in 
a  thick  unbedded  mass,  over  which  the  upper  layers  pass  on  a  considerable  curve. 

Passing  by  the  Milwaukee  region  for  the  moment,  we  find  near  Cedarburg  and 
Grafton,  excellent  examples  of  the  irregular  nature  of  this  deposit.  At  the  village  of 
Cedarburg,  most  of  the  rock  is  a  soft,  porous,  granular,  minutely  crystalline,  dolomite, 
varying  in  color  from  white  to  light  cream.  Occasionally,  cavities  of  the  size  of  a 
walnut  or  larger  appear,  but  they  are  not  frequent.  The  beds  are  from  2  feet  to  4%  feet 
thick,  but  not  well  defined,  nor  are  vertical  fissures  regular  or  prominent.  The  local 
dip  varies  from  lc  to  3j/£°  in  a  southwesterly  direction,  but  is  changeable. 

Other  portions  are  harder  and  more  compact,  some  of  which,  however,  when  mined 
back  from  the  exposed  surface,  become  softer  and  more  granular,  at  variance  with  the 
usual  fact. 

A  half  mile  to  the  east,  near  the  center  of  Sec.  26,  a  very  soft  crystalline  rock,  called 
sandstone,  from  its  friable  and  granular  nature,  occurs,  having  a  strong  dip  to  the  west- 
ward. Following  down  the  stream  a  short  distance,  we  find  a  hard,  brecciated  and  geodif- 
erous  rock  of  bluish  cast  without  apparent  stratification. 

This  gives  place  almost  immediately  to  a  granular  rock  similar  to  the  preceding,  but 


NIAGARA  LIMESTONE.  353 

the  bedding  joints  become  entirely  lost,  and,  in  an  exposure  of  20  feet,  none  are  visible. 
Vertical  seanis  occur  at  intervals,  which  are  disposed  to  change  to  an  angle  of  45°  with 
the  horizon,  and  to  pass  obliquely  across  to  the  neighboring  fissure. 

If  we  pass  on  eastward  about  half  a  mile,  we  find  a  rock,  at  a  somewhat  higher  ele- 
vation, of  a  more  earthy  structure,  belonging  to  the  Guelph  horizon,  but  when  we  reach 
the  Milwaukee  river,  below  the  rapids,  we  again  find  the  granular  rock,  as  before,  but 
distinctly  bedded  and  dipping  northward.  In  a  few  rods,  the  layers  become  harder  and 
are  almost  as  soon  lost  in  a  brecciated,  unstratified  mass,  whose  superior  hardness  has 
given  rise  to  the  rapids.  This  mass  is  made  up  of  fragments  of  rock  cemented  by  com- 
minuted debris  of  a  dolomitic  character,  winch  renders  the  distinction  of  the  fragments 
from  the  matrix  often  obscure.  This  breccia  graduates  almost  imperceptibly  into  hard, 
compact  layers,  as  we  proceed  up  the  river,  and  these  in  turn  soon  give  place  to  granular 
rocks  again,  the  strata  dipping  northward  for  a  distance,  and  then  rising,  as  illustrated 
in  the  accompanying  figure. 

FIG.  44. 


PROFILE  SECTION  ALONG  THE  MILWAUKEE  KIVEB,  BELOW  GRAFTON,  SHOWING  THE  CHANGEABLE 

NATURE  OF  THE  RACINE  LIMESTONE. 
a.  Soft  and  granular;  b.  Close-grained  and  hard;  c.  Brecciated;  d.  Hard  and  compact;  e.  Granular. 

At  the  dam  near  the  south  line  of  the  S.  E.  qr.,  Sec.  24,  Grafton,  the  granular  dolom- 
ite is  developed  hi  its  most  characteristic  form,  becoming  a  well  marked  calcareous  sand- 
rock. 

Above  the  dam,  a  harder  rock  of  closer  but  irregular  texture  ensues,  but  at  a  some- 
what higher  level,  and  belongs  to  the  Guelph  horizon. 

Near  the  center  of  the  east  line  of  Sec.  33,  Cedarburg,  there  is  an  outlier  of  rough,  coarse 
brecciated  dolomite  of  light  gray  color.  It  is  composed  of  fragments  of  compact  rock, 
the  spaces  between  which  are  filled  with  a  yellow  pulverulent  material.  As  the  rock  of 
the  vicinity  has  been  swept  away,  leaving  it  about  30  feet  higher  than  its  base,  it  is  prob- 
able that  it  was  surrounded  by  the  softer  granular  beds  that  are  prevalent  in  tin's  neigh- 
borhood. 

Throughout.  Ozaukee  and  Washington  counties,  this  formation  is  chiefly  represented 
by  rocks  similar  to  those  already  described,  but  to  this  remark  there  are  conspicuous  ex- 
ceptions. 

Near  the  south  line  of  the  S.  W.  %  of  Sec.  35,  Germantown,  there  is  a  quarry  of 
considerable  lateral  extent,  though  it  exposes  but  about  8  feet  vertically.  In  the  western 
portion  of  the  quarry,  the  upper  13  inches  consist  of  a  hard,  close-textured  rock,  but 
full  of  rough,  irregular  cavities.  Below  this,  and  not  definitely  separated  from  it,  are 
23  inches  of  porous,  granular  rock  of  the  Racine  type,  showing,  on  the  weathered  edge, 
oblique  and  cross  lamination,  (e  of  Fig.  45.)  Below  this,  are  5  feet  of  bluish  white, 
very  fine  grained,  compact  dolomite,  in  beds  averaging  6  inches  hi  thickness,  (f  of 
Fig.)  The  distinction  between  this  and  the  rock  above  is  sharp  and  clear,  so  that  it 
may  be  accurately  traced,  even  where  the  bedding  joint  does  not  correspond  to  the  junc- 
tion. Traced  to  the  northeast,  the  porous  layer  of  the  Racine  type  is  reduced  to  ]  8 
inches?  within  25  paces.  It  has  also  lost  much  of  its  porous  character,  having  changed 
so  as  to  be  less  different  from  the  upper  portion,  and  being  now  broken  up  into  irregular 
layer*.  Five  paces  farther,  this  layer  is  reduced  to  six  inches,  and  has  still  farther 
changed  in  character.  (y.)  Ten  paces  farther,  it  is  no  longer  recognizable,  both  it  and 


364 


GEOLOGY  OF  EASTERN  WISCONSIN. 


m 


the  layer  above  having  changed  so  as  to  be  scarcely  distinguish  - 
able  from  the  compact  rock  below.  Farther  on,  the  difference 
becomes  still  less,  a  few  cavities,  and  a  slightly  greater  irregu- 
larity in  the  subordinate  layers,  being  all  that  distinguishes 
them  from  the  layers  below,  (h.)  At  the  farthest  point  t:> 
which  these  layers  can  be  traced,  no  geologist  would  think  of 
separating  them  from  the  layers  below,  thus  making  it  a  clear 
case  of  thinning  out  and  transformation.  These  layers  are  es- 
sentially horizontal. 

If  we  now  return  to  the  point  in  the  southwestern  part  of  the 
quarry,  whence  we  started,  and  take  69  paces  to  the  southwest, 
we  find  the  rock  exposed  in  the  road  as  f ollows : 

First,  a  compact  limestone,  similar  to  that  in  the  quarry,  dip- 
ping eastward  at  an  angle  of  6°.  The  upper  layer  is  8  inches 
thick,  underlaid  by  one  of  4  inches,  (d.)  The  rock  for  5  paces 
is  then  covered,  beyond  which  it  again  appears.  The  upper  2'2 
inches  of  this  are  divided  irregularly  into  beds,  the  superior  por- 
tion of  which  is  as  compact  as  any  seen  at  the  quarry,  but  the 
lower  is  somewhat  more  porous.  This  dips  11°  N.  of  E.  Under 
this  lie  5  niches  of  porous  rock,  but  not  of  the  most  pronounced 
class.  Under  this,  again,  He  2  inches  of  similar  kind;  beneath 
which,  again,  there  are  5^  inches  of  limestone,  containing1 
]r,any  cavities  of  the  size  of  an  almond,  and  similar  to  the  upper 
layer  described  at  the  quarry.  Under  this  he  18%  inches  of  the 
more  pronounced  and  typical,  porous,  granular  rock,  (c.)  Hero 
again  the  section  is  interrupted  by  8  paces  of  unexposed  surface, 
when  a  porous,  granular  rock  succeeds,  having  a  dip  of  14°  N. 
of  E.  (6.)  There  are  about  26  inches  of  this,  the  irregularity  of 
the  structure  making  it  difficult  to  measure  exactly.  Below  this 
come  6  to  8  inches  of  a  rough,  irregular,  brecciated,  rather 
hard  and  tough,  but  somewhat  porous,  rock,  containing  large 
and  small  crinoid  stems,  like  those  common  in  the  Racine  beds. 
The  section  is  again  interrupted  for  4  paces,  when  a  rough,  very 
irregular,  brecciated,  porous  rock  follows,  constituting  a  confused 
mass,  similar  to  the  rock  mounds  near  Milwaukee  and  Wauwa- 
tosa,  yet  to  be  described,  (a.)  In  this,  Illcenus  ioxus,  fragments 
of  Atrypa  and  Rhynchonella,  crinoid  stems,  and  an  Orthoceras, 
were  found.  This  exposure  continues  18  paces.  The  whole  sit- 
uation is  imperfectly  represented  by  the  accompanying  figure. 

It  seems  to  be  possible  to  draw  but  one  rational  conclusion 
from  the  foregoing  facts,  viz:  (1)  That  the  last  mentioned  irreg- 
ular mass  stood  as  a  reef  in  the  depositing  sea;  and  (2)  that  the 
alternating  layers  were  deposited  on  its  slope,  while  (3)  these, 
in  the  more  quiet  waters  at  a  little  distance  from  the  reef,  were 
replaced  by  a  deposit  of  finer  silt,  which  formed  the  compact 
layers.  The  unusual  phenomena  of  cross  and  oblique  lamina- 
tion in  limestone  harmonizes  with  this  view. 

Within  a  mile  from  this  point,  there  are  several  exposures  of 
the  compact  rock.  In  the  south  half  of  Sec.  36,  this  even  tex- 
tured, compact  variety  is  associated  with  a  layer  of  the  same 
general  color  and  composition,  but  having  a  sort  of  lumpy 
structure,  a  kind  of  conglomerate,  in  which  the  pebbles  and 


NIAGARA  LIMESTONE.  365 

matrix  were  of  the  same  material,  and  blended  in  solidification.  This  association  here 
is  an  important  link  in  the  chain  of  evidence,  as  we  have  a  precisely  similar  association 
with  even  textured  layers,  near  Milwaukee,  which  have  been  heretofore  excluded  from 
the  Racine  group. 

The  position  of  these  beds  is  also  to  be  taken  into  account.  To  the  northeast,  north- 
west, southwest  and  southeast,  are  outcrops  of  the  characteristic  granular  rock,  within 
from  one  to  four  miles,  with  nothing  in  the  topography  to  favor  any  other  view  than 
that  taken. 

About  four  miles  to  the  southeast  (middle  N.  line  Sec.  29,  Granville,  Milwaukee 
county),  we  find  a  mound  of  confused,  unstratified  rock,  having  a  north  and  south  axis. 
The  rock  is  dirty  buff  in  color,  and  soft,  granular,  arid  almost  pulverulent  in  texture. 
Eighty-five  paces  to  the  southeast  of  this,  is  a  similar,  but  much  smaller,  mound,  on 
the  north  side  of  which  a  quarry  has  been  opened  in  even  bedde'd,  rather  soft  and  porous 
dolomite,  the  layers  of  which  dip  into,  or  under,  the  mound  at  an  average  angle  of  about 
4°.  Penfci»ieruf>  (Gypidula )  multicostata  abounds  in  these  layers,  and,  in  the  larger 
mound,  is  associated  with  other  Niagara  fossils. 

Near  Milwaukee  there  are  three  mounds  or  ridges  of  rock  that  have  attracted  much 
attention,  and  which  seem  to  be  regarded  as  exceptional  phenomena,  but  which,  I  think, 
in  the  light  of  preceding  and  subsequent  facts,  should  cease  to  be  so  regarded.     One  of 
jji       .»  these,  known  as  Moody 's  quarry,  is  located  in 

the  Fourth  ward  of  the  city  of  Milwaukee,  in 
the  side  of  the  bluff  facing  the  Menomonee 
river.  Another  is  situated  in  the  grounds  of 
the  National  Military  Asylum,  and  the  chief 
and  most  noted  at  the  station  Raphu,  near 
Wanwatosa,  and  commonly  referred  to  the 
SQOWING  THE  STRATIFICATION  AT  MOODY'S  ]atter  locality  in  the  literature  of  the  subject. 

The  distance  from  the  first  to  the  second,  on  an 

air  line,  is  2^  miles;  from  the  second  to  the  third,  a  little  more  than  two  miles,  and 
from  the  first  to  the  third,  less  than  3j^  miles.  Lines  joining  them  thus  would  form  an 
obtuse-angled  triangle.  Within  this  triangle  are  two  quarries  of  regularly  bedded, 
horizontal  limestone.  One  of  these,  Storey's  quarry,  is  about  two-thirds  of  a  rnilu 
northeast  of  the  outcrop  in  the  Asylum  grounds,  and  the  other,  about  the  same  distance 
from  the  Raphu  or  Wauwatosa  mound.  Only  a  few  rods  west  of  the  last,  there  are  sim- 
ilar horizantal  beds,  having  a  very  close  relationship  to  the  mound.  These  mounds  are 
similar  in  character.  The  most  striking  peculiarity,  aside  from  their  external  form  and 
stratigraphical  relations,  is  the  great  irregularity  of  their  structure.  The  stratification 
is  obscure,  and  sometimes  apparently  wanting.  The  rock  has  an  irregular  texture  and 
varying,  but  frequently  glassy,  fracture,  and  contains  many  cavities  of  varying  size  and 
very  irregular  form.  These  are  sometimes  drusy  with  crystals,  sometimes  coated  with 
stalagmite,  or,  again,  filled  with  pulverulent  material.  The  color  is  also  varying,  but  usu- 
ally bluish  or  yellowish.  In  composition,  it  is  nearly  a  pure  dolomite,  and  that  from 
Schoonmaker's  quarry  is  used  successfully  as  a  flux  for  iron  at  the  Bay  View  furnaces. 

As  the  quarries  near  Wanwatosa  furnish  the  best  exposures,  are  the  most  fossilifer- 
ous,  and  have  been  the  subject  of  most  discussion,  it  is  desirable  that  we  should  enter 
somewhat  into  particulars  in  reference  to  this  interesting  locality.  If  we  place  ourselves 
at  the  extreme  western  exposure,  known  as  Busack's  quarry  (see  Fig.),  we  shall  find  a 
section  showing  heavy,  well  defined,  nearly  horizontal,  slightly  argillaceous  beds,  of  a 
rather  fine,  uniform,  compact  grain,  medium  hardness,  smooth  conchoidal  fracture,  and 
bluish  gray  color.  Interstratified  with  these?  are  layers  having  the  lumpy  nature  pre- 
viously described  as  occurring  in  Sec.  36,  Germantown.  The  layers  dip  eastward  to 
about  the  middle  of  the  quarry,  from  which  they  rise,  but  not  uniformly,  for  at  this 


366 


GEOLOGY  OF  EASTERN  WISCONSIN. 


point  an  east  and  west  axis  occurs,  having  the  general  trend  of  the  ridge  farther  east, 
and  with  which  it  probably  has  a  definite  connection.  An  east  and  west  section  in  this 
part  of  the  quarry  would  show  a  dip  to  the  westward,  and  a  north  and  south  section  woul.1 
exhibit  the  layers  curving  gently  over  this  axis.  But  as  we 
trace  the  rock  eastward,  it  changes  in  nature.  Near  the  east- 
ern extremity,  the  upper  layer  becomes  slightly  irregular  in. 
bedding,  and  rather  soft,  and  granular  in  texture. 

Below  this  is  a  layer  from  22  to  24  inches  thick,  divided 
into  sublayers,  somewhat  irregularly,  and  occasionally  show- 
ing Lines  of  deposition.    To  casual  observation,  it  appears  to 
be  a  compact,  fine-grained,  even-textured  dolomite,   but 
closer  inspection  shows  it  to  contain  many  small  cavities, 
that  are  angular  and  sharply  defined,  and  are  the  result  of 
the  removal  of  minute  fossils,  in  which  the  rock  abounds  at 
this  point.     Aside  from  these,  the  rock  is  as  previously  de- 
scribed, with  occasional  seams  of  argillaceous  material.     Be- 
.    low  this,  the  rock  is  similar  to  that  in  the  western  part  of  tho 
§     quarry.     In  the  extreme  southeastern  portion  exposed  in  con- 
i    nection  with  this  quarry,  the  rock  becomes  quite  irregular  iii 
>=    structure. 

There  ensues  at  this  point,  unfortunately,  an  interruption 
i  of  several  rods  in  the  exposure,  so  that  this  incipient  change 
•  in  structure  cannot  be  traced  to  its  consummation. 

Passing  this  interval,  we  find  at  the  western  extremity  of 
!    Mr.  Schoomnaker's  quarry,  at  the  surface,  a  cellular,  even 
§    textured,  regularly  bedded  rock,  similar  to  the  last  described, 
^    but  of  Lighter  color,  and  more  distinctly  granular  imture. 
g    This  dips  southward  at  an  angle  of  about  15°.     As  the  face 

5  of  the  quarry  curves  round  to  the  south,  the  whole  section  is 
§    composed  of  similar  rock  down  to  and  beneath  the  water 

(  that  occupies  the  bottom  of  the  quarry  at  this  point.  But 
§  these  lower  layers  dip  less  and  less,  until  they  become  hori- 
g  zontal,  and  even  slightly  incline  toward  the  irregular  mass. 
o  If  we  trace  these  lower  layers  toward  the  ridge,  their  inclina- 
H  tion  somewhat  increases  as  well  as  their  thickness  —  this 
•>  latter  sometimes  markedly  —  until  they  are  lost  in  the  ob- 
>  scure  structure  of  the  reef,  or  disappear  at  the  surface, 
g  As  we  pass  eastward  along  the  face  of  this  ridge,  now  well 
;5  exposed  by  quarrying,  the  dip  of  the  ill- defined  layers  in- 

6  creases  gro  dually  to  54°,  when  the  stratification  can  no  longer 
be  clearly  distinguished.     This  obscurity  continues  for  80 
paces.    There  are  some  indications  of  horizontal  bedding  in 
this  space,  and  also  some  that  the  dip  is  to  the  south,  and. 
that  the  exposure  is  along  the  strike  of  the  strata,  but  neither 
observation  is  altogether  trustworthy. 

East  of  this,  blue  and  lighter  colored  bands  indicate  a  dip 
of  about  30°  eastward.  This  continues  for  about  35  paces, 
the  observation  at  the  eastern  extremity  showing  a  dip  of 
31°  in  a  direction  E.  10°  to  15°  S.,  this  being  the  dip  as  ex- 
posed, not  necessarily  the  full  amount  of  the  true  dip.  The 
same  qualification  is  true  of  the  other  observations  made  en 
dip  along  the  face  of  this  exposure. 


NIAGARA  LIMESTONE.  367 

Ten  paces  of  unexposed  face  succeeds,  followed  by  90  paces  uncovered,  which  shows  an 
obscure  dip  of  about  30°  E.  of  S.  Again  30  paces  are  concealed,  bej»ond  which  a  face  40 
yards  in  length  succeeds,  whose  dip  is  33°  E.  of  S.  After  another  interruption  of  60 
paces,  we  find  the  last  exposure  of  about  10  paces  length,  whose  very  obscure  strati- 
fication indicates  a  dip  to  the  S.  W.  The  ridge  reaches  a  hight  of  about  45  feet  above 
the  sole  of  the  quarry. 

Near  the  summit  of  the  ridge,  at  its  western  extremity,  is  a  slight  outcrop  apparently 
in  place,  and  seeming  to  dip  to  the  northwestward  (20°,  N.  30°  W.).  If  this  be  reliable, 
we  should  infer  that  the  ridge  was  comparatively  narrow,  as  the  exposure  lies  only  17 
paces  back  from  the  face  of  the  quarry. 

The  trend  of  the  ridge,  as  estimated  from  the  exposures,  is  a  little  to  the  north  of 
east. 

The  rock  at  Storey's  and  Schwickhart's  quarries,  within  the  triangle  before 
mentioned,  is  closely  similar  to  that  in  the  western  part  of  Busack's  quarry,  and  the 
same  remark  may  be  made  of  the  fossils,  which  consist  mainly  of  Orthoceratites. 
But  in  Busack's  quarry,  where  the  strata  approach  the  reef,  the  fauna  is  much  ampli- 
fied, and  we  find  Halt/sites  catenulatus,  an  undetermined  Trematopora,  Streptelasma 
and  Fenestella,  Stephanocrinus  gemmiformis,  Orthis  biloba,  0.  elegantula,  Strophomeiia 
rhomboidalis,  Streporhynchus  subplanum,  Atrypa  reticularis,  Rhynchonella  neglecta, 
Platyceras  Niagarense,  Ortliocems  annulatum,  a  new  species  of  Phragmoceras,  found 
also  in  the  adjoining  reef,  a  Gomphoceras,  Calymene  Niagarensis,  Encnnurus  omatus, 
and  a  new  species  found  also  at  Zimmerman's  quarry,  Illcenus  loxus,  and  Bronteus 
Acamas. 

From  all  the  foregoing  facts,  it  may  be  regarded  as  fairly  demonstrated  that  theso 
horizontal  beds  were  laid  down  simultaneously  with  the  formation  of  the  mounds.  Tho 
cellular  nature  of  the  rock  of  the  latter,  and  the  uncompressed  condition  of  fragile  fos- 
sils, are  fatal  to  any  theory  of  upheaval,  or  other  violent  action. 

About  five  miles  northwest  of  this,  at  Zimmerman's  quarry,  in  Section  7,  N.  E.  qr., 
Wauwatosa,  there  is  an  even-bedded  limestone  of  compact  or  minutely  cellular  texture, 
very  similar  to  that  of  some  layers  in  the  eastern  part  of  Busack's  quarry  already  de- 
scribed, and  to  which  they  are  equivalent,  as  shown  by  the  contained  fossils.  As  quar- 
ried, the  layers  are  thin,  but  the  true  beds  are  of  more  considerable  thickness,  a  state- 
ment which  is  true  of  most  or  all  the  flags  and  apparently  thin-bedded  strata  of  this 
region.  A  few  miles  farther  to  the  northwest,  at  Howard's  quarry,  and  at  several 
other  points  in  Menomonee,  quarries  of  white  and  gray  flags,  and  even-bedded,  com- 
pact, fine-grained,  chertless  limestones  occur,  that  seem  to  belong  to  this  horizon.  At 
Howard's  are  found  Halysites  calenulatus,  Atrypa  nodostriata,  OrtJwceras  annulatum, 
0.  medulare,  Phragmoceras  Nestor,  Illcenus  loxus,  Calymene  Niagarensis,  and  several 
undetermined  forms.  At  other  points,  fossils  are  rare.  In  the  adjoining  town  of  Lisbon, 
as  already  mentioned,  are  similar  strata,  whose  exact  stratigraphical  position  is  some- 
what doubtful.  From  the  fact  that  the  compact,  even-bedded  rock  that  unquestionably 
belongs  to  the  Racine  horizon  is  evervwhere,  so  far  as  known,  free  from  chert,  while 
the  strata  immediately  underlying  the  undoubted  Racine  beds  at  Waukesha  are  highly 
cherty —  and  the  same  is  true  of  the  layers  beneath  the  Racine  in  all  the  northern-  coun- 
ties —  the  presence  or  absence  of  chert  is  entitled  to  some  consideration  as  a  d  istinguish- 
ing  feature.  From  its  nature,  however,  I  am  disinclined  to  rigidly  apply  it  as  a  diag- 
nostic character,  and,  besides,  such  application  would,  in  some  cases,  lead  to  strati- 
graphical  difficulties.  It  may  be  best,  however,  to  provisionally  regard  the  chertless 
beds  as  belonging  to  the  Racine  horizon,  and  the  cherty  flags  to  the  Waukesha  beds. 
If  this  rule  be  followed,  most  of  the  rock  exposed  in  the  town  of  Lisbon,  and  a  portion 
of  that  in  Pewaukee,  would  bo  regarded  as  Racine.  In  justification  of  the  fact  that  any 
doubt  remains,  it  is  to  be  remarked  that  this  is  a  region  of  almost  universally  prevalent 


368  GEOLOGY  OF  EASTERN  WISCONSIN. 

drift,  and  that  exposures  of  the  rock  are  few  and  of  limited  extent,  and  it  is  further  to 
be  remembered  that  these  are  distinctions  between  subordinate  divisions  of  the  same 
epoch,  and  involve  discriminations  not  often  attempted  with  equal  detail. 

In  the  norlhsrn  counties,  the  formjtion  is  nrich  m:>re  uniform,  both  in  the  character 
of  the  rock  and  of  its  organic  contents.  As  a  type,  or  at  least  standard  of  comparison, 
we  may  select  a  limited  but  characteristic  section  from  the  town  of  Kewaunee  (T.  23, 
R.  24,  Sec.  14,  S.  hf). 

1.  Top  Layer.     A  hard,  compact,  rather  fine-grained,  grayish  white,  even 

bedded  dolomite,  of  somewhat  uneven  texture,  weathering  into 
creases,  rather  than  pits,  and  quite  fossiliferous,  especially  abound- 
ing in  Brachiopods 1  ft  10  in. 

2.  Somewhat  similar  to  the  above,  but  coarser,  softer,  more  uneven  in 

texture,  more  inclined  to  be  granular,  and  containing  fewer  fossils. 

It  weathers  into  pits  rather  than  creases 1  ft    2  in. 

3.  Similar  to  the  last,  but  still  more  soft  and  granular,  and  more  irregu- 

lar in  bedding  and  texture 2  ft    4  in. 

4.  Similar  to  the  above 3  ft    6  in. 

5.  Thin  layers,  belonging  to  the  Upper  Coral  beds 11  ft. 

Although  some  of  these  layers  are  described  as  soft  and  granular,  they  do  not  possess 

these  qualities  in  the  same  degree  as  that  at  Cedarburg  and  similar  localities. 

At  Wilmot's  quarry  S.  E.  qr.,  Sec.  32,  Pierce  (T.  24,  R.  24),  about  five  miles  from  the 
above,  we  find  a  rather  soft,  somewhat  granular  dolomite  of  subcrystalline  structure,  ir- 
regular fracture,  rather  thick,  scarcely  even  beds,  of  bluish  and  grayish  white  color, 
with  occasional  stains  of  yellow  and  red,  weathering  to  a  yellow  or  buff. 

All  of  the  rock  referred  to  this  formation  in  Kewaunee  county  is  very  similar  to  the 
above. 

One  more  example,  from  near  Sturgeon  Bay,  Sec.  9,  S.  E.  qr.,  T.  27,  R.  26,  will 
suffice  for  this  portion  of  the  formation.  This  outcrop  consists  of  a  -vhitish,  somewhat 
granular,  porous  dolomite,  of  subcrystalline  structure.  It  is  heavy  bedded  and  weathers 
into  pits  and  creases,  but  not  conspicuously  so.  The  weathered  surface  shows  white 
lines  about  one-half  inch  in  width  that  are  usually  parallel  to  the  bedding.  These  cor- 
respond to  thin  laminae  of  a  more  compact,  homogeneous,  cryptocrystalline  rock,  appar- 
ently of  essentially  the  same  chemical  composition  as  the  rest.  Some  portions  of  the 
rock  instead  of  being  granular,  are  close  and  flintlike  in  texture,  although  enclosing 
numerous  small  cavities.  On  the  average,  the  rock  is  of  medium  hardness  and  irregular 
fracture. 

The  formation  throughout  Door  county  does  not  essentially  differ  from  this,  except 
that  at  some  points  it  verges  more  toward  the  coarse-grained  saccharoidal  marbles. 

Speaking  in  general  terms,  the  formation  is  possessed  of  quite  constant  lithological 
characters  north  of  Sheboygan  county. 

Summation.  It  appears,  then,  that  in  the  southern  counties  there 
are  three  well  marked  classes  of  limestones,  with  intermediate  grada- 
tions, one  class,  consisting  of  very  irregular,  often  brecciated  or  con  • 
glomeritic  dolomite,  forming  masses  that  usually  appear  as  mounds, 
or  ridges  of  rock,  of  obscure  stratification,  a  second  class,  formed  of 
pure,  soft,  granular  dolomites,  a  part  of  them  calcareous  sandrock, 
and  a  third  class,  consisting  of  compact,  fine  grained,  regular,  even 
beds.  We  have  demonstrated  that  the  three  forms  change  into  each 
other  when  traced  horizontally.  They  were  therefore  formed  simul- 


NIAGARA  LIMESTONE.  369 

taneously.  The  view  that  best  explains  these  facts  is,  (1)  that  the 
mounds  and  ridges  were  ancient  reefs,  and  (2)  that  the  granular  sand 
rock  was  formed  from  calcareous  sands,  derived  by  wave-action  from 
the  reef,  and  (3)  that  the  compact  strata  originated  from  the  deposit 
of  the  finer  calcareous  mud  that  settled  in  deeper  and  more  quiet 
waters,  the  whole  process  being  analogous  to,  if  not  identical  with,  the 
coral  formation  of  the  present  seas.  But  before  pursuing  this  analogy 
farther,  it  will  be  well  to  consider  the  evidences  of  life  found  in  these 
rocks.  While  some  of  the  reefs,  or  at  least  that  portion  of  them  that 
happens  to  be  exposed  to  examination,  present  only  a  few  fragments 
of  fossils,  others  are  prolific  in  organic  remains,  and  some  of  them  are 
remarkable  for  the  richness  and  variety  of  their  fauna.  The  reef  near 
Wauwatosa  (Schoonmaker's  quarry),  is  a  striking  instance  of  this. 
There  have  been  collected  from  it,  chiefly  by  Dr.  Day,  probably  not 
less  than  two  hundred  species.  Of  these  there  have  been  identified 
28  Corals,  8  Bryozoans,  4  Crinoids,  19  Brachiopods,  11  Gasteropods, 
9  Lamellibranchs,  24  Cephalopods,  and  16  Trilobites.  And  an  ex- 
haustive examination  of  the  collections  would  doubtless  much  increase 
the  number.  The  specific  character  of  these  will  be  seen  by  consult- 
ing the  accompanying  table.  This  locality  is  especially  notable  for 
its  Trilobites.  At  the  quarry  in  Milwaukee,  Corals  are  proportion- 
ately more  abundant  in  number  of  individuals.  At  Noessen's  quarry 
near  Saukville,  where  there  is  a  mingling  of  Racine  and  Guelph 
faunas,  some  portions  of  the  rock  are  little  more  than  a  mass  of  coral 
remains  imbedded  in  calcareous  sand. 

Of  the  granular  varieties  of  rock,  that  which  is  nearest  allied  to  the 
reef  rock  is  peculiarly  notable  for  an  abundance  of  Crinoids.  The  lo- 
cality near  Racine  is  preeminent  in  this  respect.  Upwards  of  thirty 
species  have  been  identified  from  this  one  locality.  These  are  associ- 
ated, as  will  be  seen  by  consulting  the  table,  with  a  large  number  of 
Corals,  Brachiopods,  Gasteropods,  Cephalopods,  Trilobites  and  a  lesser 
number  of  other  forms.  Very  similar  faunas  are  displayed  at  Green- 
field, Waukesha,  and  elsewhere.  The  more  purely  granular  sandrock 
seldom  contains  many  fossils. 

The  fauna  of  the  compact  strata  is  distinguished  for  the  conspicu- 
ous presence  of  the  straight  and  curved  Cephalopods  with  compara- 
tively few  associates.  The  Cephalopods  are  abundant,  as  already 
noted,  in  the  reefs  and  crinoid  beds,  but  are  overshadowed  by  the 
number  and  variety  of  other  forms,  while  in  the  compact  rock,  they 
greatly  predominate. 

It  appears  then,  (1)  that  upon  the  reefs  there  swarmed  a  vast  variety 
of  life;  (2)  that  upon  certain  banks  or  shoal  areas  there  was  also  great 
Wis.  SUE.  — 24 


370  GEOLOGY  OF  EASTERN  WISCONSIN. 

abundance  and  variety,  among  which  the  crinoid  family  attained  un- 
usual  prominence;  (3)  that  over  areas  of  submarine  sand-flats  there 
either  was  little  life  present,  or,  from  the  porous  nature  of  the  rock,  it 
has  been  illy  preserved,  and  (4)  that  over  the  deeper  areas,  that  de- 
posited fine  calcareous  mud,  the  gigantic  Cephalopods  held  sway. 
The  counterpart  of  all  this  is  to  be  found  among  the  coral  reefs  of  to- 
day. Vivid  descriptions,  almost  specifically  applicable  to  the  forma- 
tions in  question,  save  in  the  modern  aspect  of  the  life,  may  be  found 
in  the  writings  of  Prof.  Dana  and  Mr.  Darwin  on  recent  coral  forma- 
tions. A  few  quotations  from  the  excellent  work  of  the  former  on 
Corals  and  Coral  Islands,  may  find  a  place  here  by  way  of  illustration 
and  confirmation. 

"Generally  the  barren  areas  much  exceed  those  flourishing  with  zoophytes,  and  not 
unfrequently  the  clusters  are  scattered  like  tufts  of  vegetation  in  a  sandy  plain.  The 
growing  corals  extend  up  the  sloping  edge  of  the  reef,  nearly  to  low  tide  level.  For  ten 
to  twenty  yards  from  the  margin,  the  reef  is  usually  very  cavernous,  or  pierced  with 
holes  or  sinuous  recesses,  a  hiding  place  for  crabs  and  shrimps,  or  a  retreat  for  the  echini, 
asterias,  sea-anemones  and  mollusks;  and  over  this  portion  of  the  platform  the  gigantic 
Tridacna,  sometimes  over  two  feet  long  and  five  hundred  pounds  in  weight,  is  often 
found,  lying  more  than  half  buried  in  the  solid  rock,  with  barely  room  to  gape  a  little 
its  ponderous  shell,  and  expose  to  the  waters  a  gorgeously  colored  mantle.  Further  in 
are  occasional  pools  and  basins,  alive  with  ah1  that  lives  in  these  strange  coral  seas. 
The  reef  rock,  when  broken,  shows  commonly  its  detritus  origin.  Parts  are  of  compact, 
homogeneous  texture,  and  solid  white  limestone,  without  a  piece  of  coral  distinguishable, 
and  rarely  an  imbedded  shell.  But  generally  the  rock  is  a  breccia,  or  conglomerate, 
made  up  of  corals  cemented  into  a  compact  mass,  and  the  fragments  of  which  it  con- 
sists are  sometimes  many  cubic  feet  in  size."  "Besides  corals,  the  shells  of  the  seas  con- 
tribute to  it,  and  it  sometimes  contains  them  as  fossils,  along  with  bones  of  fishes, 
exuvia  of  crabs,  spines,  and  fragments  of  Echini,  Orbitolites  (disk-shaped  foraminifers), 
and  other  remains  of  organic  life  inhabiting  reef  grounds." 

Speaking  of  the  masses  of  coral  rock  thrown  upon  the  beach  by  the 
waves,  he  says: 

"  On  moving  these  masses,  which  usually  rest  upon  their  projecting  angles,  and  have 
an  open  space  beneath,  the  waters  at  once  became  alive  with  shrimps,  crabs  and  fish, 
escaping  from  then:  disturbed  shelter:  and  beneath  appear  various  Actiniae,  or  living 
flowers,  the  spiny  echini  and  sluggish  biche-de-mar,  while  swanns  of  shells,  having  each 
a  soldier  crab  for  their  tenant,  walk  ott  with  unusual  life  and  stateliness.  Moreover, 
delicate  corallines,  Ascidise  and  sponges  tint  with  lively  shades  of  red,  green  and  pink, 
the  under  surface  of  the  block  of  coral  which  had  formed  the  roof  of  the  little  grotto." 

In  other  portions  of  the  same  work,  there  are  frequent  descriptions 
or  references  to  sandrock,  solid  limestone,  and  various  conglomeritic 
forms,  that  might  almost  have  been  embodied  as  a  portion  of  the  lith- 
ologicnl  description  of  this  exposure  of  the  Racine  limestone.  It  does 
not  appear,  however,  that  Corals  played  so  conspicuous  a  part,  relat- 


NIAGARA  LIMESTONE,  371 

ively,  in  the  formation  of  these  ancient  reefs  as  they  do  in  modern 
ones.  In  the  northern  counties,  the  Racine  strata  present  no  indica- 
tions of  this  reef  formation,  but  in  Ozaukee  and  Washington  counties 
it  becomes  pronounced  and  extends  thence  southward  until,  south  of 
Racine,  the  formation  is  concealed  completely  beneath  the  drift.  The 
line  of  reefs  is  unquestionably  sixty  miles  in  length,  and  may  be 
much  more.  From  their  position  they  must  be  regarded  as  of  the 
nature  of  barrier  reefs.  It  is  worthy  of  remark  here  that  the  reefs 
terminate  at  the  north  at  that  point  at  which  the  underlying  forma- 
tions undergo  the  modifications  previously  described,  and  it  is  partic- 
ularly worthy  of  notice  that  this  is  the  point  where  the  Waukesha  beds 
give  place  to  the  Byron  and  Coral  beds,  from  which  it  appears  that 
the  discrimination  of  these  subdivisions  has  an  historical  and  dynam- 
ical importance.  The  consideration  of  the  industrial  value  of  this 
formation  will  be  found  following  the  treatment  of  the  Guelph  beds. 
Dr.  F.  H.  Day,  of  Wauwatosa,  through  years  of  industrious  accu- 
mulation, has  gathered,  from  the  several  localities  of  this  formation 
in  the  southeastern  part  of  the  state,  a  very  extensive  collection,  that 
is  exceedingly  rich  in  new,  interesting,  and  typical  forms.  He  has 
very  kindly  furnished  the  survey  a  list  of  species  found  at  the  several 
localities,  which  is  incorporated  in  the  following  table.  The  species 
given  on  the  authority  of  Dr.  Day  are  marked  thus  f,  those  of  the 
survey,  thus,  *. 


372  GEOLOGY  OF  EASTERN  WISCONSIN. 

FOSSILS  OF  THE  RACINE  BEDS  OF  THE  NIAGARA  GROUP. 


GENERA  AND  SPECIES. 

Burlington. 

« 
P3 

Greenfield. 

Waukesha. 

Wauwatosa. 
(Zimmerman's.) 

Wauwatosa. 
(Schoonmaker's.) 

Milwaukee. 
(Moody's.)  1 

Menonionee  Falls. 

Grafton. 

Kewaunee. 
(Sec.  14.) 

Kewaunee. 
(Wilmot's.) 

£ 

m 
g 

& 
I 

02 

PLANTS. 

f 

Buthotrephis,  und.  sp  

* 

t 

t 

t 

t 

FORAMINIFERA. 

Receptaculites  hemispheri- 
cus  

t 

t 

t 

t 

* 
* 

* 

R.     infundibulifortnis  .... 

PETROSPONGIA. 

Stromatopora  concentrica. 

CORALS. 

t 

t 
t 

t 

*t 
*t 

4 

t 
*t 

* 

* 

*t 

*t 

4 

* 

* 

Astrocerium  constrictum  .  . 

*t 

t 
*t 

4 

*t 

A.    venustuin  

* 
* 

* 

Halysites  catenulatus  

*t 

* 

t 

* 

* 

* 

-j- 

* 

Heliolites  pyrif  ormis  

* 

*t 
+ 

* 

H.  macrostylus  

Thecia  und  sp  

+ 

t 

Cladopora  reticulata  

f 

*t 

t 

+ 

* 
* 

* 

S.    verticillata  

* 

Diphyphyllum  csespitosum. 
D.    sp.,  with  larger  col's.  . 

* 

t 
+ 

* 

* 

D.     sp.,  with  smaller  col's. 

* 
* 

* 

*t 

* 

+ 

* 

* 

* 

* 

Amplexus  Shumardi  

*t 

*t 

* 

t 

* 

Zaphrentis,  und.  sp  

t 

t 

t 

t 

* 

* 

* 

t 

* 

* 

t 

t 

t 

* 

Aulacophyllum,  und  sp  .  .  . 

.^jQyathoxonia  Wisconsmen- 

* 

Chonophyllum  Niagarense. 
Cystiphyllum  Niagarense.  . 

+ 

t 

t 

* 

* 

* 

* 

.... 

Strombodes  pentaaronus  .  . 

*•• 

NIAGARA  LIMESTONE. 


373 


FOSSILS  OF  THE  RACINE  BEDS  OP  THE  NIAGARA  GROUP  —  continued. 


GENERA  AND  SPECIES. 

Burlington. 

c' 

Greenfield. 

Waukesha. 

Wauwatosa. 
(Zimmerman's.) 

Wauwatosa-. 
(Schoonmaker's.) 

Milwaukee. 
(Moody's.) 

Menomonee  Falls. 

Graf  ton. 

Kewaunee. 
(Sec.  14.) 

Kewaunee. 
(Wilmot's.) 

& 

m 

o 

0) 

B 

3 

45 
02 

CRINOIDEA. 

*t 
*t 

*t 
*t 
*t 
*t 

*t 

*t 

* 
' 

* 

T 

• 

i 

; 
• 

*t 
*t 

f 

Marcrostylocrinus  striatus  . 
Melocrinus  Verneulii  .... 

*t 

*t 

*t 

t 

.... 

.... 

.... 

G      nobilis  

G     pentan  oTilaris  •  • 

f 

Eucalyptocrinus  coslatus  •  • 

* 

n 

*t 

*.. 
*.  . 

*" 

; 

*: 

• 

• 
• 

t 

t 

i 

f 

E.    cornutus,var.  excavat's 
E     crassus  

f 

E      obconicus  

•• 

1 

*.. 

*t 
t 

*.. 

*t 
*t 

Stephanocrinus  gemmifor- 

* 

*t 

* 

Ichthyocrinus  subangularis 

CYSTIDEA. 

f 

t 

f 

*" 

t 

t 

*t 

n 
•f 

*t 

t 
t 

t 

Hemicosmites  subglobosus 
Holocystites  cylindricus  .  .  • 

*t 
*t 

* 

*t 

4 

H      Winchelli  

t 
t 

"f 

t 
* 

I 

t 
*t 

BRTOZOA. 

Lichenalia  ccncentrica.  .  .  . 
Sagenella  rnembranacea  .  . 



t 

t 
*t 

*t 
* 

* 

j. 

t 

t 

* 

t 

374  GEOLOGY  OF  EASTERN  WISCONSIN. 

FOSSILS  OF  THE  RACINE  BED  OF  THE  NIAGARA  GROUP  —  continued. 


GENERA  AND  SPECIES. 

Burling-ton. 

<D 

.5 
§ 
P3 

Greenfield. 

Waukf'sha. 

Wauwatosa. 
(Zimmerman's.) 

Wauwatosa. 

fSc.hnnmniilrpr'c  "l 

Milwaukee. 
(Moodv's.) 

Menomonee  Falls. 

a" 

o 

1 

o 

oT 

<D  ^~ 

§s 

Ss 

we: 

Kewaunee, 
CWilniot's.l 

£ 

»  « 

d 

1 

ZQ 

* 

BRYOZOA  —  (con.) 

t 

t 

* 
* 

* 

ERACHirODA. 

t 
*t 

.: 

Trimerella,sp.res.T.grandi 

t 
t 

f 

f 

* 

*.. 

t 

*t 

4 

*t 

* 

4 
4 

* 

* 

*•• 

* 

0     flabellula     

* 

* 

f 

* 

.... 

0     lynx     

* 

t 

0     oblata(')  

* 

* 

* 

* 

Streptorhynchus  subplanu 

* 

* 

.... 

* 

... 

.... 

* 

S     profunda  

* 

* 

* 

*9 

S           "      small  var  .  .  • 

* 
* 

* 

* 

,.. 

* 

S     rhomboidalis  

* 

* 
* 

*t 
4 

* 

... 

Leptsena  transversalis..  .  . 
Skenidium  insignum  .... 

... 

t 

*t 
* 

* 

t 

*t 
* 

* 
* 

#.  . 

•t 
t 

Spirif  era  eudora,  

S     gibbosa  

* 

t 

S     plicatella  

*t 
4 

4 

t 

4 

#.  . 
*.. 

1 

S.        "     var.  radiata  
Meristella  Hyale  

* 

* 

* 

.... 

* 

•• 

* 

* 

*9 

* 

M     nitida    •  • 

* 

* 

* 

* 

Pentasronia  n  sp   . 

* 
t 

4 

* 

Atrypa  congesta  

+ 

4 

*t 
* 

Atrypa  nodostriata  

*t 

4 

#.. 

t 

4 
* 

4 

i 

* 

A.     reticularis  

* 

* 

... 

R      Indianensis     

R     necrlecta    

*t 

* 
*? 

* 

* 

Pentamerus  fornicatus  .  . 

+ 

\ 

t 

NIAGARA  LIMESTONE.  375 

FOSSILS  OF  THE  RACINE  BEDS  OP  THE  NIAGARA  GROUP  —  continued. 


GENERA  AND  SPECIES. 

Burlington. 

OJ 

[1 

Greenfield. 

Waukesha. 

Wauwatosa 
(Zimmerman's) 

Wauwatosa, 
(  Schoonmaker  's) 

Milwaukee. 
(Moody's). 

Menomonee  Falls. 

Graf  ton. 

Kewaunee. 
(Sec.  14.) 

Kewaunee. 
(Wilmot's). 

£ 

cq 

g 
f 

§ 
c/2 

BRACHIOPODA  —  (con.) 

t 

*t 

t 

* 

* 

* 

* 

*t 

t 

t 

* 

* 
* 

* 

* 

Anastrophia  interplicata 

* 

* 

.... 

f 

\ 

\ 

t 

f 

LAMELLIBRANCHIATA. 

1 

4 

*t 

t 

Ambonychia  acutirostra  .  . 

.... 

t 

t' 
t 

* 

t 

t 

M     Nilesi 

*t 

t 

*t 

t 

Ampbicoelia  (Leptodo-     \ 

* 

mus)  Leidyi  j 
Leptodomus  undulatus,  J 

* 

."•  sp  } 

* 

4 

4 

GASTEROPODA. 

4 

M 

*t 

* 

* 

•i 

t 

* 

Platyostoma  Niagurenae   . 
Euomphalus  (Straparol-  [ 

... 

lus)  mopsus  ) 
•"¥1     Racmensis    n  sp  .    •  • 

* 

E     und  sp    ... 

* 

* 



Straparollus  solarioides  .  . 

* 

f 

t 

*j. 

t 

t 

P.    Halei  

*.. 

t 

i 

P.    Hovi  . 

t 

P.     subtilistriata  

• 

* 

* 

{ 

t 

t 

t 

t 

B.     trigonostoma  ...   .... 

* 

Cyclonema  elevatum  

* 

*t 

Loxoneina  Leda  .   

t 

t 

\ 

Bellerophon  expansus  

4 

Murchisonia  belli^incta    .  . 

t 

t 

M.     Laphami  

t 

376 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  KACINE  BEDS  OF  THE  NIAGARA  GROUP  —  continued. 


GENERA  AND  SPECIES. 

Burlington. 

0 

M 

Greenfield. 

Waukesha. 

Zimmerman's. 

Schoonmaker's. 

cc 

V, 

1 

Monomonee  Falls. 

»o 

<M 

o5 
o 

1 

O 

Kewaunee,  S.  14. 

Kewaunee, 
(Wilmot's.) 

Sturgeon  Bay. 

GASTEROPODA  —  (con.) 

t 

1- 

f 

CEPHALOPODA. 

*t 
*t 

*t 
*t 

t 

*. 
*. 
*. 
*- 

*H 
t 

A 

? 

* 

*t 

*t 

t 

* 

* 

\ 

* 

* 
• 

. 

t 

*t 

t 

Ormoceras,  sp.  res.  0.  ver- 

f 

. 

r 

* 

t 

H 

I 

H 

t 

t 

* 

* 

* 

7 

t 

f 

*t 

i 

t 
*t 

t 

? 

* 

CPotii-pri 

t 
* 

* 

* 

*t 
*\ 

\ 

t 

t 

*9 

* 

t 

\ 

T 

4 

t 

I 

t 

\ 

t 

t 

CRUSTACEA. 

t 

t 

.... 



t 

* 

* 

* 

5 

* 

j 

t 

* 

:t 

T 

*t 

* 

t 

*t 
**t' 

* 

.... 

* 

Calymene  Niagarensis.  .  . 

* 

t 

t 

7 

,1 

.\ 

*+ 

* 

NIAGARA  LIMESTONE. 


377 


FOSSILS  OF  T.HE  RACIXE  BEDS  OF  THE  NIAGARA  GROUP  —  continued. 


GENERA  AND  SPECIES. 

Burlington. 

Racine. 

Greenfield. 

Waukesha. 

,00 

<s 

a 

Schoonmaker's. 

jn 

v> 
a 

Menomonee  Falls. 

iO 
03 

6 

Ol 
OQ 

1 

O 

Kewaunee,  Sec.  14. 

Kewaunee. 

(Wilmot's.) 

£ 

« 

OJ 

I 

02 

CRUSTACEA  —  (con.) 

* 

t 

t 

\ 

* 

*\ 

\ 

$ 

1 

7 

t 

* 

Sphserexochus  Roiuingeri  . 

.     .. 

* 

.... 

9 

.... 

* 

* 

t 

t 

i» 

| 

THE  GUELPH  BEDS. 


The  Guelph  limestone  constitutes  the  uppermost  subdivision  of  the 
Niagara  Group  in  Wisconsin.  In  its  lithological  character,  it  does 
not  differ  essentially  from  the  Racine  limestone,  being  in  general  a 
rough,  thick  bedded,  irregular  dolomite,  usually  quite  free  from  im- 
purities, and  of  buff,  gray,  or  blue  color.  The  distinction  between  the 
two  subdivisions  is  a  paleontological  rather  than  a  physical  one.  In 
the  latter  respect  there  is  less  difference  between  these  than  either  of 
the  other  members  of  the  group.  There  was  evidently  no  marked 
change  in  the  physical  history  of  the  region,  but  the  same  conditions 
continued  from  the  beginning  of  the  deposit  of  the  Racine  limestone 
to  the  close  of  the  formation  of  the  Guelph  beds.  In  the  interval, 
however,  the  life  underwent  a  change  by  the  introduction  of  the 
species  that  characterize  the  Guelph  horizon.  This  introduction  was 
gradual,  so  that  many  localities  show  a  mingling  of  the  two  faunas. 
The  right  hand  white  line  on  the  maps  is  intended  to  bound  this 
formation,  and  is  drawn  so  as  to  include  localities  presenting  these 
mingled  species.  In  doing  so,  however,  it  was  necessary  to  include 
some  of  the  reefs  and  sandrock  deposits  whose  physical  history  is  un- 
questionably identical  with  the  Racine  reefs.  The  propriety  of  doing 
tliis  may  be  questioned. 

Local  Details.  The  mound  and  quarry  in  Granville  and  the  Guelph  beds  near 
Cedarburg  and  Grafton  have  been  mentioned  in  the  description  of  the  Racine  lime  • 


378  GEOLOGY  OF  EASTERN  WISCONSIN. 

stone.  In  the  former  case  the  formation  is  so  similar  to  the  reef  structure  of  the  Racino 
limestone  that  it  is  quite  possible  it  should  be  so  grouped,  as  has  been  done  in  description. 
In  the  latter  case,  however,  there  is  a  nearer  approach  to  a  lithological  distinction  than 
elsewhere,  the  Guelph  beds  being  more  regular  and  compact  than  the  subjacent  Racine. 
Gasteropods  predominate  among  the  fossils. 

At  Noessen's  quarry,  north  of  Saukville,  (Sec.  26,  N.  E.  j^),  there  is  a  limited  open- 
ing upon  an  ancient  reef,  exposing  a  rock  of  varying  character,  a  portion  of  it  being  very 
soft  and  coarsely  granular,  while  other  portions  are  compact  and  fine  grained.  Some 
portions  are  made  up  almost  wholly  of  Crinoid  stems  and  Corals,  while  others  are  brec- 
ciated.  In  color  the  rock  is  buff,  weathering  to  a  deeper  and  more  reddish  hue.  Corals 
and  Crinoids  are  abundant,  and  only  extensive  quarrying  is  needed  to  make  this  locality 
valuable  to  the  collector.  The  fauna  shows  a  mingling  of  Guelph  and  Racine  species. 
The  locality  is  rather  to  be  regarded  as  Racine  than  Guelph. 

At  the  light-house  point,  near  Sheboygan,  we  find  a  hard,  mottled,  bluish  dolomite 
of  subcrystalline,  rather  compact,  but  not  uniform  texture.  A  concentric  structure,  de- 
veloped in  blue  and  white,  is  frequent.  This  and  the  mottling,  brought  out  by  the  pol- 
ishing of  the  glacier,  and  swept  by  the  waves,  give  the  surface  a  unique  beauty.  The 
general  dip  is  to  the  southward,  but  after  passing  a  low  axis  north  of  the  point  the  slope 
is  in  the  opposite  direction.  Near  Sheboygan  Falls,  the  rock  is  similar,  though  at  a 
few  points,  a  tendency  toward  the  granular  character,  so  common  to  the  south,  is  mani- 
fested. 

At  Roth's  quarry,  N.  W.  ^  of  S.  E.  ^  of  Sec.  9,  Sheboygan,  the  greater  portion  of 
the  rock  in  the  main  quarry  east  of  the  kiln,  is  a  thick  bedded,  bluish  dolomite,  quite 
hard  and  comparatively  free  from  cavities,  but  with  occasional  geodes  of  calcite  and 
more  rarely  iron  pyrites.  Some  portions  are  beautifully  laminated.  Other  portions  are 
more  granular  and  lighter  in  color,  and  approach  somewhat  the  granular  rock  found 
farther  south.  In  general  aspect  and  lithological  character,  it  somewhat  resembles  the 
rock  of  Vaughn's  quarry,  near  Racine,  already  described.  This  and  all  the  rocks  of  this 
vicinity,  have  but  a  meagre  content  of  fossils.  A  few  rods  west  of  this,  there  occurs  a 
hard,  shaly,  bluish,  magnesian  limestone  with  argillaceous  partings  and  laminae.  Tho 
layers  are  undulating  and  the  dip  various. 

At  Rabie's  quarry  (middle  N.  %  Sec.  7,  Sheboygan),  occurs  a  rock  that  differs  from 
any  found  elsewhere  in  the  degree  of  development  reached  by  certain  tendencies  of  this 
much  varying  formation.  The  vertical  exposure  is  but  slight.  The  upper  layers  are 
rather  even  and  compact  in  texture,  but  below,  the  rock  is  highly  brecciated  with  much 
argillaceous  matter  associated  as  a  sort  of  matrix.  The  dolomite  is  a  deep  blue,  while 
the  argillaceous  matter  has  a  greenish  cast,  thus  giving  the  rock  a  much  deeper  color 
than  that  of  other  portions  of  the  formation.  These  layers  are  very  geodiferous,  the 
frequent  cavities  being  drusy  with  calcite.  The  brilliancy  of  these,  in  strong  contrast 
•with  the  deep  color  of  the  rock,  led  an  interested  party  to  believe  that  there  was  silver 
present,  and  a  little  iron  pyrites  scattered  sparsely  through  the  rock,  raised  even  brighter 
hopes,  which  we  were  seemingly  cruel,  but  really  kind,  enough  to  dissipate. 

At  Howard's  quarry,  on  the  Sheboygan  river,  the  rock  is  very  irregular,  both  in  bed- 
ding and  structure.  It  varies  from  a  soft  granular,  to  a  hard,  almost  flint-like  dolomite. 
It  contains  many  cavities,  and  weathers  to  an  exceedingly  rough,  pitted  surface.  The 
more  granular  rock  is  white,  and  the  more  flint-like,  bluish.  The  bedding  is  too  obscure 
and  irregular  to  give  any  reliable  dip.  The  rapids  here,  as  in  most  other  cases  within 
this  formation,  are  due  to  the  changeable  nature  of  the  rock,  and  not  to  the  fact  that  a 
uniformly  soft  layer  underlies  a  harder  one,  as  is  commonly  true  of  falls. 

In  the  town  of  Carlton,  Kewaunee  county,  we  find  the  most  northern  exposure  of 
this  formation  yet  recognized.  It  consists  of  a  soft,  granular,  disintegrating,  cream  or 
buff  colored  dolomite  of  irregular  bedding  and  structure.  The  fauna  is  peculiar,  in  the 
presence  of  large  Gasteropods  and  Lamellibranchs. 


NIAGARA  LIMESTONE. 


The  following  table  shows  the  character  of  the  fauna,  of  the  forma- 
tion, and  at  the  same  time  the  distribution  of  the  species  among  the 
several  localities: 

FOSSILS  OF  THE  GUELPH  BEDS  OF  THE  NIAGARA  GROUP. 


GENERA  AND  &PECIES. 

Granville,  Sec.  29.  1 

& 

o  . 

^^ 

,-  -03 

If- 

§53 

o 

rt 

o"  . 

I-IIO 
.01 

^H  . 

o 

p 

^Hi-T 

Z  ^ 

'3 

Cedai-burg,  Sec.  26,1 

E..  Y2. 

$ 

b£^ 

M 

¥. 

"?& 

0 

$ 

6 
i> 

02X  • 

^ 

ft 

^ 

o 

5, 

£^ 

rp   -f. 

fc'c 

•^  o 

i  * 

CO 

Sheboygan  Falls, 
(Howard's.) 

S 

J 
^ 

o 

PETROSPONGIA. 

* 

* 

* 

CORALS. 

* 

* 

* 

* 

*9 

* 

* 

* 

* 

* 

*9 

*0 

.  .  .  . 

* 

* 

Cladopora,  und.  sp  

* 

* 

* 

* 

* 

* 

H.    catenuiatus,  var.  microporus  

* 

Cyathophvllum,  und.  sp  

* 

* 

* 

* 

* 

* 

* 

Chonophyllum  magmficum  

*9 

Cystiphyllum,  sp.  res.  C.  Niagarense  

* 

* 

* 

* 

Zaplirentis,  und.  sp  

* 

" 

CRINOIDEA. 

Eucalyptocrinus  coelatus  

* 

E.    ornatys.  ...    

* 

Glyptocrinus  nobilis  

* 

BRACHIOPODA. 

Monomerella  prisca  

*•? 

*? 

* 

Orthis  elegantula  

* 

Strophomona  profunda  

* 

* 

S.    rhomboidalis  

* 

Spirifera  plicatella,  var.  radiata  

* 

Meristella  Hyale=Charionella  Hyale  

* 

Retzia,  uud.  sp  

* 

Atyrpa,  und.  sp  

* 

Rhynchonella  cuneata  

* 

* 

* 

R.    neglecta  

* 

* 

R.    pisuin  

* 

Pentanierus  oblongus  

* 

P.    ventricosus  

* 

* 

P.    und.  sp  

* 

* 

* 

Gypidula  (Pentameras)  multicostata    .... 

* 

*9 

* 

* 

G     occidentalis  

* 

* 

* 

LAMELLIBRANCHIATA. 

Me^alomus  Canadensis.       

. 

* 

Ambonychia  acutirostra  

* 

Bensselaeria,  n.  sp  

* 

380 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS   OF   THE  GUELVH   BEDS   OF  THE  NIAGARA   GllOUP —  CO)ltl)lUC(l. 


GENERA  AKD  SPECIES. 

Granville,  Sec.  29. 

« 
*S 

rH     . 
"       O 
~  O> 

J00. 

'S^H 

goa 
O 

» 

o"   . 

i—  I  lO 
r  .CM 

"       0 

I- 

g^ 

O 

o 

<M 

i 

CO 

fcic 

1* 

'gw 

O 

£ 
s 

CO     . 
8»^ 

C 

1^ 

03     . 
TScO 

8 

3 

6 

V 

1« 
|& 

1* 

a 

oO 

8 
g, 

=37 

5s 

C8   ^ 
CO 

Sheboygan.  (How- 
ard's.) 

cd 
oa 

1 
1 

i 

O 
* 

GASTEROPODA. 

* 

* 

* 

* 

* 

* 

* 

* 

* 

* 
* 

* 

* 

* 
* 
* 

1VI     lonsrispira  . 

*9 

* 

* 

* 

* 

Pleurotomaria  axion  

* 

P.    Halei  

* 
* 

* 

P.    idia  

* 

* 

Straparollus  Hippolyte  

* 

* 

* 

Trochonema  Fatua  

* 

Subulites  ventricosus  

* 

CEPHALOPODA. 

.-  Orthoceras  abnorme  

* 

* 

'  O.    annulatum  

* 

* 

<t-^Or*  Carltonense,  n.  sp  .   

* 

* 

0.    crebescens  

* 

Gomphoceras,  und.  sp  

* 

Cyrtoceras  arcticameratum  

* 

C.    laterals  

* 

f,  --C;    rectum,  n.  sp  .  

C.    rigidum  

* 

Phratpnoceras,  und.  sp  

* 

CRUSTACEA. 

Illaenus  loxus  

* 

Bronteus  Acamas  

* 

INDUSTRIAL  VALUE  or  THE  WAUKESHA,  KACINE  AND  GUELPH  BEDS. 

Lime.  Probably  the  Niagara  limestone  surpasses  all  other  forma- 
tions in  the  interior  of  the  continent,  in  the  amount  and  excellence  of 
the  quick  lime  produced  from  it,  and  certainly  the  formation  no 
where  surpasses  the  purity  and  adaptation  to  lime  manufacture  that 
it  attains  within  the_region  under  consideration.  The  excellence  of 


NIAGARA  LIMESTONE.  381 

certain  portions  of  the  lower  members  in  this  respect  has  already  been 
considered,  and  the  higher  members  now  claim  attention. 

The  following  analyses  show  that  the  first  great  essential,  purity,  ia 
possessed  in  a  high  degree: 


Carbonate  of  lime       

I. 
52.86 

II. 
52.16 

III. 
55.23 

IV. 
55.41 

42.98 

43.50 

43.52 

43.48 

0.10 

0.05 

0.12 

0.10 

0.32) 

0.82 

0.92 

0.61 

0.50 

Trace 

Trace 

Water  

0.49 

0.67 

0.25 

Insoluble  residue  

,  3.44 

0.28 

0.40 

Total   

100.09 

99.65 

100.47 

100.00 

~No.  1  is  from  the  Pentamerus  layer  at  Pelton's  quarry,  Pewaukee. 
This  layer  is  not  now  burned  for  lime,  the  upper  layers,  which  are 
purer,  being  used  exclusively.  No.  II  is  from  Mr.  Horlick's,  and 
No.  Ill  from  Mr.  Beswick's  quarries,  Racine.  All  the  foregoing 
analyses  are  by  Prof.  Daniells.  No.  IY  is  an  average  of  six  analyses 
of  as  many  layers  of  Mr.  J.  Druecker's  quarry,  near  Port  "Washing- 
ton, by  Mr.  Bode.  It  will  be  observed  that  the  average  insoluble  res- 
idue of  those  that  are  used  for  lime  is  less  than  one-half  of  one  per 
cent.;  or,  if  the  alumina  and  iron  be  included,  but  little  over  one  per 
cent.  These  are  not  analyses  of  exceptional  specimens,  but  are  be- 
lieved to  be  fair  averages  of  the  rock  used  for  the  market  product,  and 
inexhaustible  quantities  of  equally  excellent  material  are  readily  acces- 
sible. The  material  used  by  the  leading  lime-burners  at  other  points 
is  of  essentially  the  same  excellent  quality. 

Aside  from  chemical  purity,  a  certain  degree  of  porosity  is  desira- 
ble, since  it  promotes  the  ready  escape  of  the  gases  and  secures  a 
uniform  and  complete  reduction  without  an  excessive  heat  and  the 
consequent  partial  vitrification  of  the  surface  and  loss  of  strength. 
It  likewise  facilitates  complete  slacking  when  used,  thus  tending  to 
reduce  the  liability  to  slack  in  the  wall,  which  is  the  annoying  habit 
of  some  limes  when  carelessly  used.  The  more  minutely  and  uni- 
formly porous  the  rock  is,  the  better.  The  formation  under  consid- 
eration presents  abundant  deposits  that  possess  this  desirable  quality 
in  an  eminent  degree,  and  this  kind  of  rock  is  now  almost  exclusively 
used,  the  practical  experience  of  burners  having  led  to  this,  without, 
perhaps,  fully  appreciating  the  reason  for  it. 

Owing  to  these  excellencies,  the  Wisconsin  limes  produced  from 


382  GEOLOGY  OF  EASTERN  WISCONSIN. 

this  formation  enjoy  a  high  reputation,  and  are  largely  used  in  the 
Chicago  market,  notwithstanding  the  distance.  When  visited,  the 
kilns  of  Messrs.  H.  &  Y.  C.  Pel  ton,  of  Pewankee,  were  producing 
1,200  barrels  per  week,  which  was  shipped  to  Chicago,  Grand  Haven, 
Sparta,  Des  Monies  and  elsewhere.  At  the  kilns  of  Mr.  Ormshy,  of 
the  same  place,  2,000  barrels  were  being  burned  per  week,  about  one- 
half  of  which  was  shipped  to  Chicago  and  the  rest  mainly  to  the  La 
Crosse  region.  Messrs.  Colville  &  Ormsby,  of  Lisbon,  were  burning 
700  barrels  per  week.  Messrs.  Horlick  &  Sons,  of  Racine,  manufac- 
ture from  60,000  to  75,000  barrels  per  year,  which  is  sent  to  the  west 
and  south,  and  to  Michigan.  Their  business  is  so  extensive  as  to  re- 
quire a  branch  house  in  Chicago.  Mr.  Beswick,  of  the  same  place, 
burns  upward  of  18,000  barrels  per  year,  which  is  used  chiefly  at  points 
on  the  Lake  Shore  railroad.  Mr.  Vaughn,  of  the  same  place,  pro- 
duces from  600  to  1,000  barrels  per  week,  which  is  mostly  sold  at 
Chicago.  At  Waukesha,  the  Messrs.  Hadfield  burn  and  ship  exten- 
sively. Mr.  Johnson,  in  the  town  of  Genesee,  burns  sufficient  to  sup- 
ply the  local  demand.  Mr.  Trimbone,  of  Greenfield,  produces  from 
60,000  to  80,000  barrels  per  year,  which  is  chiefly  consumed  in  Mil- 
waukee. The  kiln  of  Mr.  Druecker,  near  Port  Washington,  has  a 
capacity  of  250  barrels  daily,  the  product  of  which  is  shipped  to 
Chicago.  At  Mr.  Roth's  kilns,  near  Sheboygan,  1,600  to  1,700  bar- 
rels per  year  are  produced.  At  numerous  other  points,  there  are 
kilns  of  capacity  sufficient  to  supply  the  local  demand.  Probably 
400,000  larrels  may  be  considered  a  fair  estimate  of  the  total  amount 
of  lime  burned  per  year  from  the  Niagara  limestone. 

Building-Stone.  While  this  district  yearly  exports  large  quanti- 
ties of  brick  and  lime,  it  continues  to  import  more  or  less  of  build- 
ino-  stone.  This  is  due  less  to  the  necessities  of  the  case  than  to  the 

O 

want  of  development  of  our  own  resources  So  far  as  there  may  be  a 
demand  for  silicious  sandstone,  there  will  probably  continue  to  be  a 
a  necessity  for  going  outside  of  our  district,  though  not  outside  of  the 
state,  but  the  formation  under  consideration  is  capable  of  furnishing 
excellent  material  for  both  massive  and  ornamental  construction. 

The  careful,  and  in  many  cases,  elaborate  descriptions  of  the  texture 
and  bedding  of  the  members  of  the  formation,  given  under  the  head  of 
local  details,  need  not  be  repeated,  and  our  attention  may  be  confined  to 
a  few  localities  that  especially  deserve  mention.  The  quarries  of  the 
Messrs.  Hadfield,  near  Waukesha,  afford  excellent,  compact,  fine- 
grained, white,  or  light-gray  beds,  20  inches  or  more,  in  available 
thickness.  The  rock  has  a  reliable  conchoidal  fracture  and  can  be 
dressed  with  as  much  ease  and  facility,  as  is  attainable  in  so  firm  a 


NIAGARA  LIMESTONE.  353 

rock.  It  is  admirably  adapted  to  use  as  dimension  stone  of  various 
kinds,  particularly  for  trimmings  with  white  brick,  with  which  its 
color  harmonizes  beautifully. 

A  white  and  most  excellent  rock  of  similar  texture  is  wrought  at 

o 

Johnson's  quarry,  Genesee,  and  is  worthy  of  high  commendation. 

Near  Cedarburg,  at  the  quarry  of  Messrs.  Schleifer  &  Anshuetz,  a 
white,  granular,  crystalline  rock  occurs  in  massive  deposit  without  ev- 
ident bedding  joints,  so  that  blocks  of  any  required  dimensions  can  be 
obtained.  It  cuts  with  great  facility  and  is  a  beautiful  stone.  Large 
quantities  are  shipped  to  Milwaukee,  and  the  surrounding  country. 

At  Kuntz'  quarry,  Manitowoc,  a  compact,  fine-grained,  crystalline 
dolomite  of  excellent  quality  has  been  mined  to  some  exent,  and  even 
sawed  and  polished  as  a  marble.  While  not  suited  to  polishing,  it  is 
excellent  for  the  coarser,  ornamental  purposes.  In  Cooperstown  and 
elsewhere  very  fine  dolomites  await  development. 

Gen.  Q.  A.  Gilmore,  in  his  work  on  Building  Stone,  gives  the 
crushing  strength  of  a  two  inch  cube  of  bluish  drab  limestone,  from 
Sturgeon  Bay,  as  86,000  pounds  on  bed,  and  66,750  on  edge,  with  the 
comment,  "  a  remarkably  solid,  stable  stone."  That  of  the  white  Jol- 
iet  (111.)  limestone,  sometimes  imported,  he  gives  as  ranging  from 
45,000  to  67,000  on  bed.  In  addition  to  the  fine  qualities  of  rock,  the 
formation  furnishes  unlimited  quantities  of  material  suitable  for 
rough-dressed,  course  work,  and  the  heavier  class  of  masonry. 

Flux.  The  limestone  from  Schoomaker's  quarry,  west  of  Milwau- 
kee, is  used  successfully  as  a  flux  in  the  Bay  Yiew  Iron  Works,  and 
the  limestones  from  Trimbone's  and  Druecker's  quarries  have  been 
also  tested  with  favorable  results.  The  pure,  granular  limestones  in. 
the  towns  of  Cedarburg,  Graf  ton  and  Germantown,  may  also  be  recom- 
mended. 


384: 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  NIAGARA  GROUP. 


GENERA  AND  SPECIES. 

Author 
of 
Species. 

r§ 
1 
j» 

! 
a 

OD 

H3 

3 

a 
I 

m 

OJ 

o> 

i 

h 
1 

3 

Upper  Coral  beds. 

Waukesha  beds. 

Racine  beds. 

CO 

•T3 
<D 

"S. 

'a; 

a 
O 

;  Not  observed. 

PLANTS. 

* 

* 

FORAMINIFERA. 

Receptaculites  hemisphericus.  . 

Hall 

* 

Hall     .  * 

* 

PETROSPONGIA. 

Stromatopora  concentrica  .... 

CORALS. 

Goldfuss  
Goldfuss  

* 
* 

.... 

* 
* 

* 

* 
* 

* 
* 

* 
* 

* 

.... 

F  .    Gothlandicus  ?  (large  cells)  . 

* 
* 

HaU  

* 

• 

* 
*9 

* 
* 

* 
* 

Sav.  . 

* 

* 

F.     clavate  form,  2  kinds  cells  . 

* 

Hall  

* 

* 

* 

* 

* 
* 

*? 

.... 

Hall  

* 

* 

* 

* 

Mich.  &  Hind. 

* 

Thecia,  und.  sp.  with  small  cells. 

* 
* 

* 
* 
* 

Hall  

Hall       .  .     . 

* 
* 
* 
* 

* 
* 
* 

» 

* 

* 

* 
* 
* 

* 
* 



/Jff  r  catenulatus  var.  microporus 
yxH.  t  catenulatus  var.  macroporus 

Hall       .     .  . 

* 

Guettard  
Hall           

* 

* 
* 

*'? 

* 

* 

* 

* 

* 

* 

* 

S     retiformis 

* 

* 

* 

Diphyphyllum  csespitosum  

Hall  

* 

.... 

* 

* 

* 
* 

* 

.... 

* 

* 

* 
* 
* 

* 

.... 

* 

* 

* 

* 

* 

* 

# 
* 

* 
* 

* 

.... 

Hall     

Zaphrentis,  sp.  res.  Z.  gigantea  . 

Ed.  andHaine 
Hall 

*    1 

* 

* 

Z.    und.  sp.  .  . 

HaU    . 

* 

• 

* 

* 

NIAGARA  LIMESTONE. 
FOSSILS  OF  THE  NIAGARA  GROUP  —  continued. 


385 


GENERA  AND  SPECIES. 

Author 
of 
Species. 

03 

'  vj 

J 

o> 

& 
& 

0 

O) 
.£> 

el 

« 

*  *  Lower  Coral  beds. 

-3 

<v 

i 

o 
o 

Ll 

1 

& 

p 

Waukesba  beds. 

OT 

T3 

8 
^ 

<B 

1 
w 

Guelph  beds. 

Not  observed. 

CORALS  —  (con.) 

- 

* 

* 

/^fiyathaxonia  Wisconsinensis  .  . 
Chonophyllum  magnificum.  .  .  . 

n.  sp  

... 

* 

• 

... 

Hall  

* 

* 

* 

* 

* 

.... 

* 

.... 

Hall  

Cystiphyllum  Niagarense  
Cystiphyllum  und  sp  

Hall  

* 

* 

* 

.... 

bcronibocles  pentagonus      .... 

Goldfuss  

* 

* 

S     n  sp  .       . 

• 
# 

j/^ystostylus  typicus  

CRINOIDEA. 

* 

Stephanocriiius  gemmiforniis.  . 

Hall  .  . 

* 

Hall  

* 

* 

Macrostylocrinus  striatus  

Hall  

* 

Melocrinus  Verneuili  

Troost  

* 
* 

Hall  

Hall  

• 

E.    cornutus,  var  excavatus  .  . 

Hall  

* 

Hall  

* 

Hall  

* 

E.    ornatus  

Hall  

* 

E.    n.  sp  

* 

Glyptocrinus  arniosus  

McChesney 

* 

G.    nobilis     

Hall  ' 

* 

Lampterocrinus  inflatus  

Hall  

* 

(.ilyptaster  occidentahs  

Hall  

* 

Hall...    . 

* 

Rhodocrinus  rectus  

Hall  

* 
* 

R.    sculptilis  

Hall  

Cyathocrinus  Cora  

Hall  

* 

Cyathocrinus  pisit'ormis  

Rcemer  

* 

C.    Waukoma  

Hall  

* 

Say  ...     . 

* 

* 

* 

Cryptodiscus  

CYSTIDEA. 

Holocystites  abnorruis  

Hall  . 

* 
* 

H.     alternatus  

Hall  

H.    cylindricus   

Hall  

* 

H.    ovatus  

Hall  

* 

H.    scutellatus  

Hall  

* 

H.    Wincbelli  

Hall  

* 

Gompbocystites  clavus  

Hall  

41 

G.    glans  

Hall  

* 

Hemicosmites  subglobosus  .... 

Hall  

* 

Apiocystitcs  imago  

Hall.. 

* 

Wis.  SUR.  —  25 


386 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  NIAGARA  GROUP  —  continued 


GENERA  AND  SPECIES. 

Author 
of 
species. 

4 

^ 

CD 

1 
& 

T§ 
1 

S 
>> 
M 

o5 
T3 
CD 
^5 

^ 
§ 

o 

LI 

S 

1 

Upper  Coral  beds. 

Waukesha  beds. 

CO 

T3 
co 

ft 
CD 

d 

Guelph  beds. 

Not  observed. 

OYSTIDEA  —  (COn.) 

HaU  

* 

Hall  

* 

* 

BRYOZOA. 

Hall  

* 

Sairenella  membranacea  

Hall  

* 

Fpnestella  elegans  

Hall  

* 

* 

Polypora  incepta  

Hall  

* 

* 

* 

BRACIIIOPODA. 

* 

Dinobolus  Conradi  

Hall  

* 

Monomerella  prisca  

Rillincrs      .  .  . 

* 

Trinierella  grandis  '  

* 

Orthis  biloba    

* 

0.    ele^antula  

* 

* 

0     flabellula     

Sowerby   .  .  . 

* 

* 

* 

• 

0     hybrida     

*9 

* 

0     lynx  

Eichwald 

* 

Streptorhynchus  subplarium-  •  . 

* 

* 

Hall  

* 

S     profunda  

Conrad 

*9 

* 

*•) 

S     rhoinboidalis  

^Vahlenberef 

* 

* 

* 

* 

Hall  

* 

* 

Strophodonta  striata  

Hall  

* 

* 

Leptsena  transversalis  

Wahl    

* 

Skenidiuni  insignuin  '  

Hall    .. 

* 

Spiriiera  eudora  

Hall.   .. 

* 

Hall  

* 

Hall  

* 

Hall  

* 

Si     nobilis  

Barrande 

* 

S.    plicatella  

Soweiby   .... 

* 

S.    plicatella,  var.  radiata-  •  •  . 

* 

* 

S     sp  und  

* 

Meristella  Hyale  =  Charionella 

Billings     .... 

*9 

Billinfs 

* 

Hall  &  

* 

M.    Maria  

Hall  

* 

Hall     . 

* 

* 

Pentagonia,  sp.  und  

* 

Hall  

* 

Retzia    aprinis  =  Atrypa    and 
Rhynchonella  aprinis  

Hall  

* 

... 

* 

* 

Atrvpa  nodostriata  

* 

* 

NIAGARA  LIMESTONE. 


387 


FOSSILS  OF  THE  NIAGARA  GROUP  —  continued. 


GENERA  AND  SPECIES. 

Author 
of 

Species. 

00 

'C 

Byron  beds. 

Lower  Coral  beds. 

Upper  Coral  beds. 

Waukesha  beds. 

-/' 

5 

| 

1 

^ 
1 

a 

o 

;  Not  observed. 

BRACHIOPODA  —  (COn.  ) 

* 

* 

* 

* 

* 

* 

* 

A.     reticularis  

* 

* 

.... 

Rhvnchonella  cuneata  • 

Dalman  
Hall 

* 

R.     Indianensis  
R.    neglecta  

Hall  
H.&W  

* 
* 

.  •  •    . 

Eichwaldia  reticulata  
Pentamerus  bisulcatus  

Hall  
McChesney.  .  . 
Hall  

* 

* 

* 

* 

P.    oblongus  

Murchison  .  .  . 
H.  &  W  
Hall  

*? 

.... 

* 
* 
* 

* 

* 

* 

* 

... 

P.    pergibbosus  
P.     ventricosus   
P.     und.  sp  
P.    new  sp  

* 

* 

* 

* 

.... 

Gypidula  occidentalis  
G.    multicostata  
Stricklandinia  Galtensis?  
^48.    multilirata  
S.    undet.  sp  

Hall  
Hall  
Billings  

* 

* 

* 

S.    new  sp  

Leptocoelia  planoconvexa  

Hall  
Hall 

* 

* 

L.    phcatula  

Porambonites  punctostriata  ?= 

Hall 

* 

Orthis  punctostriata  

LAMELLIBRANCHIATA. 

* 

* 

* 

Pterinea  brisa  

Hall       .     .. 

Hall 

P.     undata  

Hall 

* 

* 

Hall 

A.    aphea  •  ?  

Hall 

Hall 

* 

M.    Nilesi=Edmondia  Nilesi 

Wfr  TVT 

* 

Hall 

* 

Hall 

* 

Leptodomus  Leidyi= 

Hall 

* 

* 

* 

Hall 

* 

Hill 

* 

* 

GASTEROPODA. 

Hall 

* 

Platyceras  Niagarense  

Hall  

* 

* 

.... 

E.    (Straparollus)  mopsus  .  .  . 

Hall 

* 

*? 

* 

* 

.... 

Straparollus  Hippolyte  

Hall  

* 

t 

3SS 


GEOLOGY  OF  EASTERN  WISCONSIN. 


FOSSILS  OF  THE  NIAGARA  GROUP  —  continued. 


GENERA  AND  SPECIES. 

Author 
of 
Species. 

Mayville  beds. 

a; 
TJ 

OJ 

^5 

fl 

E 
>« 

M 

Lower  Coral  beds. 

Upper  Coral  beds. 

Waukesha  beds. 

Racine  beds. 

•/' 

"T3 

1 

Jl 

ro! 

o 

Not  observed. 

GASTEROPODA  —  (con.) 

* 

Meek  .  .  . 

* 

Hall   

* 

* 
* 

HolopGa  clGVttta        •            .... 

Hall   

* 

Billing's   .    .  . 

* 

Hall   

• 

* 

Hafl 

* 

Hall   

* 
* 

* 

P     Fatua 

Hall   

P     Halei  .                    ... 

Hall   

# 
* 

* 

* 

P     Hovi 

Hall  

P      Idia 

Hall   

* 

* 

* 

Hall 

* 

Hall   

* 

Hall  

* 

ji  gp    

* 

Billings   

* 

* 

* 

Hall   

* 

Hall   

* 

Hall   

>:= 

Hall   

* 

M      Mylitta 

Billing's   

* 

Hall   

* 

Loxoneina  Leda 

Hall  

* 

i\  gp  

* 

Hall 

* 

H  &  W  .   ... 

* 

Metoptonia  sp  und 

* 

Hall 

* 

* 
* 

CEPHALOPODA. 

Orthoceras  abnonrie  

Hall 

* 
* 
* 

0     alienum  

Hall   ... 

* 

* 
* 

0.    annulatum  
>/0     Carltonense    

Sowerby  

* 
* 

... 

O.    columnare  
0     crebescens  

Hall  
Hall     .  . 

.... 

* 
* 

* 

# 

* 

* 

0     Hoyi  

0.     Laphami  

Hall   

* 

0     medulare  

Hall 

# 

* 
* 

Hall 

Ormoceras,  sp.  res.    0.  verte- 

* 

Hall   . 

* 

Discosorus  conoideus  

Hall  
Hall   

* 

* 
* 

Hall 

* 

* 

G.    und.  sp  

NIAGARA  LIMESTONE. 


FOSSILS  OF  THE  NIAGAKA  GROUP  —  continued. 


GENERA  AND  SPECIES. 

Author 
of 

Species. 

GO 

^5 
J 

o> 

1 
s 

-3 

<u 

-Q 

d 

I 

Lower  Coral  beds. 

00 

•a 

o> 

f 
Is 
8 
O 

1 

& 

Pi 

o 

Waukesha  beds. 

Racine  beds. 

•/' 

'C 

0) 
^3 

j3< 
'oS 

3 

o 

:  Not  observed. 

CEPHALOPODA  —  (con.) 

Hall  

* 

Hall   

* 

* 

Hall  

C     Foster!                

Hall    

* 

* 

Hall  

if 

* 

Hall   

* 

Hall   

* 

* 

* 

.... 

Hall  

* 

Hall  

* 

* 

P     Nestor        .       . 

Hall   

* 

* 
* 

... 

.... 

Gyroceras  Hercules  

W.  &M  
Hall  

.... 

.... 

.... 

* 

* 

McClies  ney 

* 

Meek  

* 

Hall  

* 

* 

* 

CRUSTACEA. 

Leperditia  fonticola    

Hall  

* 

Hall  

* 

* 

Hall   

* 

H  &  W  ..   .. 

* 

Hall   

* 

Hall   

* 

# 

Hall  

* 

* 

* 

jl    gn  

* 

* 

* 

* 
* 

# 
* 

* 

• 

Hall  

•  • 

-• 

Hall   

Hall  

Hall  

Hall   

* 

H  &  W     

* 

* 
* 
* 

Hall   

* 

Hall 

Hall   

* 

... 

* 

* 

« 

... 

Hafl   

* 

390  GEOLOGY  OF  EASTERN  WISCONSIN. 


LOWER  HELDERBERG  LIMESTONE. 

Four  miles  northwest  of  the  city  of  Milwaukee  —  Sec.  7,  town  of 
Wauwatoaa  —  in  the  banks  of  Mud  Creek,  are  two  low  exposures  of  a 
shaly  limestone,  that  differs  in  lithological  character  from  both  the 
Niagara  limestone,  upon  which  it  rests,  and  the  Hamilton  cement 
stone,  by  which  it  is  overlaid.  The  rock  is  a  hard,  brittle,  light  gray, 
magnesian  limestone,  distinguished  by  numerous  minute,  angular 
cavities,  that  give  to  it  a  very  peculiar,  porous  structure.  It  is  thin- 
bedded  and  laminated,  by  virtue  of  which  it  splits  very  readily  into 
flags  and  thin  plates,  which  are,  for  the  most  part,  too  brittle,  and  too 
much  subject  to  further  splitting,  to  be  serviceable  as  paving,  but 
which  are  considered  valuable  for  Macadamizing.  A  transverse  frac- 
ture of  some  of  the  layers  exhibits  an  alternation  of  gray  and  dark 
colored  laminae,  peculiarly  characteristic  of  this  formation. 

The  rock  is  a  nearly  pure  dolomite,  as  shown  by  the  following  an- 
alysis, by  Mr.  Bode: 

Carbonate  of  lime 54.569 

Carbonate  of  magnesia 43.410 

Silica 1 . 494 

Alumina 0.211 

Oxide  of  iron 0.316 


100,000 

The  two  quarries  are  less  than  half  a  mile  apart,  and  lie  on  a  near- 
ly east  and  west  line.  On  this  line,  a  little  less  than  two  miles  to  the 
east,  along  the  Milwaukee  river,  a  short  distance  above  the  Washing- 
ton street  bridge,  the  Hamilton  cement  stone  is  found  to  rest  upon  a 
dark  brown,  ferruginous  rock,  that,  to  casual  observation,  bears  little 
resemblance  to  that  above  described,  but  which,  upon  closer  inspec- 
tion, is  found  to  possess,  in  a  large  degree,  the  same  peculiar  porous 
and  laminated  structure,  and  to  differ  from  it  chiefly,  in  being  a  lit- 
tle less  shaly  and  much  more  ferruginous.  Its  chemical  composi- 
tion is  shown  by  an  analysis,  by  the  above  named  chemist,  to  be  as 
follows : 

Carbonate  of  lime 54.693 

Carbonate  of  magnesia 41.818 

Silica 1.575 

Alumina 0.478 

Oxide  of  iron 1.436 

100/000 


LOWER  HELDERBERG  LIMESTONE.  391 

From  tins  it  appears  that  it  differs  from  the  rock  upon  Mud  creek 
very  slightly,  except  in  its  content  of  oxide  of  iron,  which  gives  to  it 
its  dark  brown  color.  There  can  be  no  doubt  then  that  this  is  to  be 
regarded  as  constituting  the  uppermost  portion  of  the  formation  un- 
der consideration,  which,  therefore,  immediately  underlies  the  Kam- 
ilton  strata.  The  exposure  upon  the  Milwaukee  river  is  very  slight, 
and  it  is  impossible  to  determine  whether  there  is  strict  conformabil- 
ity  between  the  Hamilton  rock  and  that  under  consideration  or  not. 
It  can  only  be  said  that  if  any  unconformability  exists,  its  amount  is 
very  slight,  as  the  dip  of  the  strata  do  not  markedly  differ. 

Extent.  These  are  all  the  exposures  of  this  rock  at  present  known 
immediately  adjacent  to  the  Hamilton  formation.  Unfortunately  al- 
most the  whole  of  this  region  is  thickly  covered  with  drift,  and  ex- 
posures of  rock  are  exceedingly  rare.  All  the  territory  that  can  safe- 
ly be  regarded  as  occupied  by  this  shaly  limestone  will  be  found  in- 
dicated by  gray  checks  on  the  accompanying  map.  As  hereafter 
stated,  it  is  probable  .from  drift  evidences  that  there  is  a  small  patch 
on  the  north  side  of  the  Hamilton  area,  but  its  precise  location  is  un- 
known. It  might  be  presumed  that  the  formation  would  occupy  a 
belt  surrounding  the  cement  rock,  a  conjecture  which  has  heretofore 
found  expression.  But  the  following  facts  forbid  such  an  hypothesis. 
At  Schwartzburg,  a  mile  north  of  the  outcrops  on  Mud  creek,  rock 
was  reached  in  the  excavation  of  a  cellar,  which  presents  all  the  litho- 
logical  characteristics  of  the  Niagara  limestone,  and  contains  Pen- 
tamerus  ventricosus,  a  Niagara  species. 

In  the  X.  W.  qr.  of  Sec.  10  and  the  N.  E.  qr.  of  Sec.  9,  of  the  town 
of  Granville,  we  find  the  most  northwesterly  known  exposure  of  the 
overlying  Hamilton  formation,  in  the  brow  of  a  hill  facing  to  the 
northwest.  Only  thirty-six  paces  down  the  gentle  slope,  from  the  Ham- 
ilton beds,  a  pit  has  been  opened  which  discloses  the  Niagara  lime- 
stone. The  vertical  distance  between  the  top  of  the  Niagara  exposed, 
and  the  bottom  of  the  quarry  of  Hamilton  rock  is  about  six  feet. 
The  intermediate  slope  is  largely  occupied  with  old  pits,  now  filled, 
but  in  the  material  thrown  from  them,  only  Niagara  and  Hamilton 
rock  was  seen.  In  the  gutter  of  the  adjacent  road,  both  the  Hamil- 
ton and  Niagara  are  shown,  with  a  vertical  distance  of  less  than  five 
feet  between  them,  and  in  the  abundant  chipstone  of  the  gutter,  there 
was  none  of  the  shaly  limestone  under  discussion.  But  it  is  a  rock 
peculiarly  liable  to  break  up  into  chipstone,  and  is  abundant  in  the 
drift  near  the  known  outcrops,  and  in  the  line  of  drift  from  them. 

In  view  of  all  these  facts,  the  shaly  limestone  must  be  regarded  as 
absent  at  this  point.  The  occurrence  of  the  Niagara  limestone  along 


392 


GEOLOGY  OF  EASTERN  WISCONSIN. 


"he  creek,  a  half  a  mile  east,  near  the  lower  face  of  the  Hamilton 
formation  confirms  this  view. 

We  find,  however,  on  the  north  side  of  the  Hamilton  area,  some  of 
the  shaly  rock  under  discussion  in  the  drift,  from  which  it  is  probable 
that  there  is  a  concealed  area  on  that  side.  This  harmonizes  witli  the 
view  taken  in  this  report,  viz.:  that  this  shaly  rock  belongs  to  the 
Lower  Helderberg  formation,  which  is  found  in  Michigan,  and  ab- 
sent in  Iowa,  according  to  the  geologists  of  those  states,  and  hence, 
must  terminate  in  the  interval,  and  it  would  seem  that  we  have  here 
the  point  of  its  disappearance.  It  is  certain,  at  least,  that  no  "  narrow 
circular  rim  "  of  the  shaly  limestone  surrounds  the  Hamilton. 

Fossils  are  very  rare  in  this  rock,  and  I  am  not  aware  that  any  have 
previously  been  reported  from  it.  A  fair  specimen  of  Meristella 
nucleolata,  an  OrtMs,  resembling  a  young  0.  oblata,  and  an  imper- 
fect specimen  of  Meristella  or  Pentamerus  were  the  only  reward  of 
repeated  and  diligent  search. 

About  one  mile  above  the  village  of  Waubakee,  in  the  town  of 
Fredonia,  Ozaukee  county,  in  the  bed  of  the  Milwaukee  river,  and  the 
vicinity,  is  a  formation  that  deserves  our  consideration  in  this  con- 
nection. On  the  north  side  of  the  river  is  a  quarry  in  which  the  fol- 
lowing section  is  exposed: 


FIG.  48. 


1.  Light  gray,  thin  bedded,  shaly  dolomite,  resembling 
that  above  described  as  occurring  at  Mud  creek,  but 
less  porous.    The  surfaces  of  some  of  the  layers  are 
covered  with  large  numbers  of  a  Leperditia,  undistin- 
guishable  from  Leperdilia  alta 2  ft. 

2.  A  layer  of  hard  dolomite,  containing  cavities,  some  5  or 
6  inches  in  diameter,  which  are  usually  filled  with  large 
crystals  of  calcite.     Leperditia  occurs  occasionally  in 

this  layer 10     in. 


3.  Alternating  thin  and  thicker  beds  similar  to  No.  1  in 
lithological  character,  but  some  layers  are  marked  with 
a  dark,  rusty  coating 2  ft.  2  in. 


4.  Similar  to  No.  2 1  ft.  2^  in. 


5.  Moderately  thick  beds  somewhat  shaly,  intermediate  in 
character  between  the  thinner  and  thicker  beds  above . .  1  ft. 

^-r-  I  Total. .  7  ft.  2%  in. 

•*T~----    "^     ™  . 


LOWER  HELDERBERG  LIMESTONE.  393 

The  remains  of  Leperditia,  found  at  this  locality,  are  very  abund- 
ant, literally  covering  the  surface  of  some  layers,  and,  to  a  greater  or 
less  extent,  disseminated  through  the  mass  of  some  of  the  beds,  but 
unfortunately  the  state  of  preservation  is  poor.  A  careful  examina- 
tion and  comparison  of  a  large  number  of  specimens  leaves  no  doubt 
that  the  fossil  is  Leperditia  alta,  or  a  very  closely  related  species. 

In  the  bed  of  the  river  a  little  above  this  locality,  very  thin  beds  of 
a  softer,  dark  dolomite,  colored  by  carbonaceous  matter,  are  found. 
Some  of  the  layers  are  marked  by  numerous  black  or  dark  brown  car- 
bonaceous laminae,  which  give  to  the  rock  an  appearance  quite  pecu- 
liar. This  carbonaceous  matter  is  evidently  derived  from  the  remains 
of  plants,  many  indications  of  which  are  present,  among  them  forms 
resembling  Sphenothallus.  In  addition  to  these,  two  species  of 
Orthis  are  found,  one  resembling  Orthis  oblata,  and  the  other  closely 
similar  to  Orthis  subearinata,  but  smaller.  Pterinea  aviculoidea,  or 
a  very  closely  allied,  if  not  absolutely  identical,  species,  an  imperfect 
Orthoceras,  and  a  doubtful  Inocaulis,  are  also  present. 

Farther  up  the  stream,  on  the  opposite  side,  a  quarry  has  been, 
opened  which  exhibits  a  more  compact,  close  textured  rock,  and  one 
intermediate  in  lithological  character  between  these  and  the  Niagara 
limestone.  No  fossils  were  found  in  it,  and  its  relationship  is  uncer- 
tain. Its  most  striking  peculiarity  is  the  strong  undulation  of  its 
strata,  which  allies  it  rather  with  the  Niagara  than  with  the  forma- 
tion under  consideracion,  whose  beds  have  never  been  observed  other- 
wise than  as  horizontal  and  perfectly  plane. 

The  composition  of  the  formation  at  this  point  is  shown  in  the 
following  table  of  analyses  by  Mr.  Bode;  No.  I  being  the  rock  asso- 
ciated with  Leperditia;  No.  II  being  that  in  which  the  cavities  filled 
with  spar  occur;  and  No.  Ill  being  the  dark  fossiliferous  rock  from 
the  river  bed: 

I.  II.  III. 

Carbonate  of  lime 53.233         56.552         52.786 

Carbonate  of  magnesia 41 .573         41 .504         43.781 

Silica 2-905  1.287  3.094 

Alumina 1-462  0-168  0.097 

Oxideofiron 0.827  0.495  0.242 

Total 100.000        100.006        100.000 


It  will  be  observed  that  they  are  all  essentially  dolomites,  with  a  small 
percentage  of  impurity,  and  that  in  composition  they  do  not  essen- 
tially differ  from  the  Mud  creek  rock. 

The  location  of  this  peculiar  deposit  adds  interest  to  the  problem 
of  its  age  and  relationship.  A  little  more  than  two  miles  to  the 


GEOLOGY  OF  EASTERN  WISCONSIN. 

southeast  (center  E.  |-  Sec.  30,  Fredonia)  is  Smith's  quarry,  where  we 
rind  a  very  soft,  porous,  granular,  friable,  cream  colored  dolomite, 
belonging,  undoubtedly,  to  the  Niagara  formation.  At  Newburg, 
three  miles  and  a  half  to  the  northwest,  occurs  one  of  the  more  com- 
mon varieties  of  the  Niagara  limestone.  To  the  south,  similar  Niag- 
ara rocks  frequently  outcrop.  To  the  northward,  there  is  heavy  drift 
for  twenty  miles.  The  deposit  under  consideration  lies  at  a  lower 
elevation  than  the  rock  at  Newburg,  and  at  about  the  same  as  that  at 
Smith's  quarry.  It  is  nine  miles  distant  from  the  lake,  and  twenty- 
six  miles  distant  from  the  deposit  on  Mud  creek.  It  is  evident  from 
these  facts  that  the  stratigraphical  relations  of  the  deposit  contribute 
nothing  but  negative  indications,  and  the  question  of  its  age  and 
equivalency  must  rest  upon  its  lithological  character  and  organic  con- 
tents. While  it  is  evident  that  neither  of  these  is  entirely  decisive, 
yet  it  is  apparent  that  the  weight  of  their  testimony  is  in  favor  of  re- 
ferring this  formation  to  the  base  of  the  Lower  Helderberg  group. 
The  same  may  be  said  of  the  formation  near  Milwaukee.  The  limited 
area  of  these  deposits,  and  their  intimate  association  with  the  Niagara 
limestone,  taken  in  connection  with  the  unusual  changeableness  of 
the  latter  formation,  both  as  respects  its  lithological  character,  and 
organic  contents,  merits  consideration  however  in  this  connection. 
On  the  accompanying  maps,  the  two  areas  will  be  found  represented 
by  checks  of  the  color  of  the  Niagara  formation,  at  once  indicating 
their  relationship  to  that  formation,  and  their  distinction  from  it. 

Economic  Considerations.  The  rock  near  Waubakee  has  been 
burned  for  lime  with  fair  success.  It  is  not,  however,  to  be  recom- 
mended for  that  purpose,  since,  in  the  vicinity,  dolomites  of  the 
Niagara  formation  of  superior  quality  abound.  Certain  layers  fur- 
nish excellent  building  material,  and  the  thinner  beds  serve  a  tem- 
porary purpose  as  flagging,  but  their  tendency  to  split  is  detrimental 
to  their  durability.  The  same  remarks  are  true  of  the  formation  near 
Milwaukee.  Both  are  very  serviceable  for  the  purposes  of  Macad- 
amizing, owing  to  their  hardness,  and,  at  the  same  time,  the  ease  with 
which  they  are  reduced  to  the  proper  form. 


PLATE.XIIiA 


HAMILTON  CEMENT  ROCK.  395 


CHAPTEE  IX. 
DEVONIAN. 

HAMILTON  CEMENT  ROCK. 

The  uppermost  and  newest  of  the  indurated  formations  of  "Wiscon- 
sin, and  the  only  representative  of  the  Devonian  age,  is  the  Hamilton 
cement  rock,  near  Milwaukee.  It  occupies  a  limited  area,  lying  adja- 
cent to  the  lake,  immediately  north  of  the  city,  and  rests  in  part  upon 
the  shaly  limestone  above  described,  and  apparently  upon  the  Niagara 
limestone  in  other  portions.  In  general  lithological  characteristics, 
it  consists  of  a  bluish-gray  or  ash-colored,  impure  dolomite,  which 
weathers,  upon  exposure,  to  a  yellowish  or  buff  color,  owing  to  the 
oxidation  of  the  iron  which  constitutes  one  of  its  ingredients.  The 
impurities  consist  chiefly  of  silica  and  alumina.  The  rock  is  char- 
acterized in  certain  portions  by  the  occasional  presence  of  cavities,  in 
which  occur  crystals  of  iron  pyrites  and  calcite,  and,  very  rarely,  zinc 
blende.  Crystals  of  the  two  former  minerals  are  disseminated  more 
or  less  through  certain  portions  of  the  rock.  In  texture,  it  is  some- 
what varying,  being  quite  homogeneous  in  some  layers,  and  quite  ir- 
regular and  lumpy  in  others,  while  the  chemical  composition  changes 
much  less  markedly,  though  sufficiently  to  affect  the  hydraulic  prop- 
erties of  the  rock.  In  degree  of  induration,  it  ranges  from  rather  soft 
to  moderately  hard.  The  beds  are  usually  thick,  with  the  exception 
of  some  portions,  which  are  somewhat  shaly.  The  general  aspect  of 
the  bedding  and  stratification  is  well  shown  in  the  accompanying 
chromo-lithograph. 

The  chemical  composition  of  the  typical  portion  is  very  fully  indi- 
cated by  the  accompanying  table  of  analyses  of  cement  rocks,  in  which 
will  be  found  eight  analyses  of  the  rock  from  the  Milwaukee  river, 
the  selections  and  determinations  being  by  different  parties. 


GEOLOGY  OF  EASTERN  WISCONSIN. 
ANALYSES  OF  CEMENT  ROCKS. 


KIND  OF  ROCK. 

/ 

Authority 
for 
analysis. 

Carbonate  of  lime. 

Carbonate  of  mag- 
nesia. 

Total  carbonates. 

ri 
_o 

02 

Alumina. 

d 

QJ 

I 

M-i 

o 
o> 

3 
'« 
0 

Total  silica,  alumi- 
na, iron,  etc. 

Milwaukee  No  1  

Bode  

45.54 

32.46 

78.00 

17.56 

1.41 

3.03 

22.00 

Bode  

48.29 

29.19 

77.48 

17.56 

1.40 

2.24 

21.20 

Milwaukee,  Layers  2—6  

Bode  

47.55 

30.91 

78.46 

13.74 

3.95 

3.85 

21.54 

Milwaukee  Layers  7—11  .    . 

Bode  

47.09 

24.95 

72.04 

18.77 

5.14 

4.05 

27.96 

Bode  

45.44 

31  .  27 

76.71 

15.65 

4.60 

3.04 

23  29 

Milwaukee  

Doremus  .  .  . 

45.57 

27.67 

73.24 

15.60 

.12 

38 

27.98 

Milwaukee,  Wash.  St.  bridge 
Milwaukee  ^V^ash    St  bridge 

Bode  
Bode  

41.34 
40.05 

34.88 
35.82 

76.22 

75.87 

16.99 
17.00 

5.00 
5.00 

1.79 

1.80 

23.78 
23.80 

Milwaukee  average  

45.11 

30.89 

76.00 

16.61 

4.09 

3.25 

24.00 

Rosendale  New  York  

Gilmore.  .  •  . 

46.00 

17.76 

63.76 

27.70 

2.34 

6.20 

36.24 

TJtica  Illinois  

Gilmore.  •  •  • 

50.42 

18.67 

69.09 

21.60 

5.27 

4.04 

30.91 

Utica,  Illinois  
Akron,  New  York  

Reid  
Gilmore  •  •  • 

58.84 
35.60 

15.38 
19.26 

64.22 

54.86 

25.20 

33.80 

6.16 
3.96 

4.40 

7.38 

35.76 
45.14 

Akron  New  York    

Reid  

35.60 

19.26 

54.86 

33.80 

3.96 

7.38 

45  14 

Sandusky  Ohio  

Reid  

40.54 

17.98 

58.52 

19.66 

3.14 

5.36 

40.26 

Points  aux  Roche,  L.Champ'n 
Cumberland,  Maryland  
English  

Reid  
Gilmore  
Berthier  .  .  . 

53.30 
41.80 
65.70 

22.60 
4.10 
0.50 

75.90 
45.90 
66.20 

20.07 
21.74 
18.00 

1.70 
16.74 
6.60 

1.70 
15.30 

8.80 

23.44 
56.78 
33.40 

Drapies    •  •  • 

61  .  60 

0.00 

61.60 

15.00 

4  80 

15.60 

35.40 

Vassy  France  •••  

63.80 

1.50 

65.30 

14.00 

5.70 

15.00 

34.70 

Theil  France  .  .  .  .  . 

Reid  

60.00 

1.32 

61.32 

18.20 

1.20 

11.28 

30.68 

Organic  Remains.  The  Hamilton  period  marked  a  new  era  in  the 
history  of  the  life  of  the  Wisconsin  formations.  While  multitudes 
of  Protozoans,  Radiates,  Mollusks  and  Articulates  lived  in  the  Sil- 
urian seas,  and  left  their  remains  embedded  and  embalmed  in  the 
accumulating  sediments,  whether  of  sandstone,  shale  or  limestone,  no 
fragment  or  trace  of  a  Vertebrate  has  been  found.  The  Hamilton 
period  witnessed  the  introduction  of  this  highest  type  of  the  animal 
kingdom  into  the  Wisconsin  series.  In  other  portions  of  America, 
the  remains  of  Vertebrates  appear  somewhat  earlier,  in  strata  wanting 
in  our  state,  and,  in  the  deposits  of  Europe,  still  earlier.  The  ver- 
tebrate remains  of  this  formation  are  confined  to  the  relics  of  fishes, 
and,  unfortunately,  these  are  fragmentary  and  imperfect.  They  have 
been  submitted  to  the  inspection  of  Dr.  J.  S.  Newberry,  a  most 
eminent  authority  in  this  department  of  paleontology,  who  finds  them 
to  be  new  and  unknown  species.  They  consist  of  fragments  of  the 
teeth  of  ChimaBroids  and  a  plate  of  a  Placoderm.  Only  one  specimen 
is  sufficiently  well  preserved  to  justify  description,  and  being  thus 
exceptional  in  character,  may  merit  the  partiality  of  delineation  here. 
The  following  is  the  description  of  Prof.  Newberry: 


HAMILTON  CEMENT  ROCK.  397 


Hhynchodus  excavatus. 

Tootli  small,  when  entire,  perhaps  two  and  a  half  inches  long  by 
one  and  a  quarter  inches  deep;  crown  alone  preserved.  Of  this,  the 
external  surface  is  marked  vertically  with  vermicular  furrows;  supe- 
rior margin  sinuous,  terminating  anteriorly  in  a  prominent  point;  the 
superior  surface  irregularly  excavated  and  roughened,  showing  two 
prominent  points,  or  tubercles,  one  on  the  middle  of  the  exterior 
margin,  the  other  on  the  inner  margin,  and  near  the  anterior  ex- 
tremity. The  inner  surface  of  the  tooth  shows  a  prominent  ridge, 
running  up  to  the  anterior  point.  This  tooth  is  evidently  fitted  for 
trituration  rather  than  cutting,  and  resembles,  in  its  general  form,  R. 
frangens  of  the  Corniferous  limestone.  It  is,  however,  much  smaller 
and  thinner,  and  the  tubercles  of  the  upper  surface  are  differently 
situated  from  what  they  are  in  the  tooth  of  that  species. 

Locality  and  formation,  Hamilton  Group.  Brown  Deer,  Mil- 
waukee county,  Wisconsin. 

In  addition  to  the  fish  remains,  there  are  the  following  inverte- 
brates: Of  Bryozoans,  a  Fenestella  and  a  tuberculated  Trematopora, 
occurring  in  massive  and  frondose  forms;  of  Corals,  the  cast  of  the 
cup  of  a  Cyathophyllum  ;  of  Brachiopoda,  a  new  species  of  Lingula, 
and  also  one  of  Discina,  Orthis  impressa,  and  an  undetermined 
Ortkis,  Strophodonta  demissa,  S.  perplana.  Chonetes  coron-ata  and  a 
species  closely  resembling  C.  deflecta,  a  Productella,  allied  to  P. 
spinulicosta,  Spirifera  mucronata,  S.  medialis,  S.  granulifera,  S. 
fornacula,  S.  pinnata,  a  species  allied  to  S.  fornacula,  but  larger 
and  one  near  S.  angusta,  Spiriferina  zigzag  r,  Cyrtina  Hamiltonensis, 
Trematospira  kirsuta,  Atrypa  reticularis,  A.  occidentalis,  Leior- 
hynchus,  resembling  L.  Kelloggi\  of  Lamellibranchs,  a  Pteronites, 
PalcBoneilo  constricta.  P.  emarginata,  a  species  allied  to  P.  plana, 
Modiomorpha  concentrica,  and  an  undetermined  species;  of  Pter- 
opods,  an  Ecculiomphalus,  closely  resembling  Euomphalus  laxus;  of 
Cephalopods,  two  new  species  of  Gomphoceras,  and  an  Orthoceras; 
and  of  Crustaceans,  Phacops  Tana. 

These  show  a  preponderance  of  Hamilton  forms,  some  of  which  are 
highly  characteristic  species,  and  occur  in  great  abundance.  With 
these  are  mingled  a  number  of  Corniferous  species,  representing  a 
lower  horizon,  and  a  few  Chemung  forms  belonging  to  a  higher 
series. 

Age.  The  foregoing  fossils  are  entirely  decisive  as  to  the  age  of 
the  formation,  and  place  it  in  the  early  portion  of  the  Hamilton 
period.  This  is  entirely  in  harmony  with  its  stratigraphical  relations 
and  with  the  general  geological  structure  of  the  interior  of  the  conti- 


80S  GEOLOGY  OF  EASTERN  WISCONSIN. 

nent,  since,  eastward  from  Wisconsin,  there  intervenes  between  the 
Hamilton  strata  and  the  Niagara  series,  the  lower  Devonian  and  the 
uppermost  Silurian  formations;  while  to  the  westward,  in  northern 
Illinois  and  Iowa,  the  Hamilton  beds  rest  directly  upon  the  Niagara 
group.  The  intermediate  formations  thin  out  and  disappear,  and,  as 
already  indicated,  the  vanishing  edge  of  the  Lower  Helderberg  strata 
barely  reaches  the  eastern  margin  of  our  state.  The  mingling  of  Cor- 
niferous  species  from  below  with  Chemung  forms  from  above  is  not 
age  of  the  only  an  interesting  fact  in  itself,  but  is  one  whose  bearing 
upon  the  deposit  is  most  significant  and  decisive,  and  establishes  the 
correctness  of  its  reference  to  the  Hamilton  period. 

Local  Descriptions.  The  most  extensive  and  important  outcrop 
of  this  formation  is  found  along  the  Milwaukee  river,  in  the  vicinity 
of  Washington  Street  Bridge,  extending  above  and  below,  in  Sees. 
4  and  5,  T.  7,  R.  22  E.  The  rock  nowhere  rises  to  any  considerable 
height  above  the  river-bed,  so  that  no  extensive  vertical  section  can. 
be  seen,  and  the  frequent  interruptions  of  the  exposure,  as  traced 
along  the  river,  prevent  any  trustworthy  correlation  of  the  strata. 
The  lithological  characters  of  the  rock  at  this  point  are  essentially 
those  before  given  as  general  characteristics,  and  this  'locality  may  be 
regarded  as  the  typical  one  of  the  formation.  A  portion  of  the  layers 
found  west  of  the  bridge  are  more  shaly  than  the  average  rock  of  the 
formation,  and  tend  to  disintegrate  somewhat  more  readily  on  expos- 
ure. A  stratum  found  below  the  bridge  possesses  a  more  granular 
character  than  the  rest  of  the  formation,  but  the  chemical  analyses 
that  have  been  made  of  the  several  portions,  indicate  that  these  varia- 
tions are  largely  of  a  physical  nature,  and  that  the  chemical  composi- 
tion is  less  varying.  In  the  drift  lying  upon  this  rock,  an  abimdance 
of  black  shale  is  present  in  thin,  fragile,  more  or  less  rounded  chips, 
indicating  the  near  presence  of  the  formation  from  which  they  are 
derived,  and  which  may  be  conjectured  to  be  the  overlying  black  slate, 
so  abundant  in  other  regions.  No  exposures  of  this  rock  have,  how- 
ever, been  discovered  in  Wisconsin,  but  as  this  region  is  extensively 
covered  with  drift,  it  is  not  impossible  that  they  exist. 

Nearly  all  the  species  of  the  foregoing  list  have  been  found  at  this 
locality,  notwithstanding  the  limited  extent  of  the  exposure,  and  indi- 
cate a  rich  and  abundant  fauna.  The  working  of  the  beds,  which  has 
been  commenced  since  this  collection  was  made,  and  the  importance 
and  interest  which  now  attaches  to  the  formation  will,  doubtless, 
very  much  increase  the  number  of  species  now  given,  and  develop 
specimens  which  will  more  fully  elucidate  the  structure  of  some  that 
are  now  imperfectly  represented. 


HAMILTON  CEMENT  ROCK.  399 

In  section  11,  town  of  Granville,  a  railroad  cut  just  south  of  the 
flag  station,  known  as  Brown  Peer,  exhibits  a  few  feet  of  this  forma- 
tion. The  original  lithological  characters  are  essentially  those  already 
described,  but  the  rock  of  this  locality  has  been  more  extensively 
weathered  than  that  near  Washington  Street  bridge,  and  presents  a 
buff  color,  except  in  the  interior  of  some  of  the  heavier  layers,  and  is 
also  somewhat  decomposed  in  certain  portions.  This  is  the  typical 
locality  of  the  Chimseroid  fish,  Rhynchodus  excavatus,  previously 
described,  and  with  it  are  associated  the  leading  forms  of  the  general 
list  above  given,  prominent  among  which  are  Orthis  impressa, 
Strophodonta  demissa,  S.  perplana,  Sperifera  pinnata,  8.  medialis, 
Speriferina  zigzag,  Atrypa  reticularis,  Palceoneilo  constricta, 
Modiomorpha  concentrica,  and  others.  It  is  stated  that  in  the  bed 
of  the  Milwaukee  river  opposite  this  point,  the  formation  exists  in 
place;  but  it  was  not  accessible  at  the  time  of  our  investigations. 

In  sections  9  and  10  of  the  same  township,  occurs  the  most 
northwesterly  exposure  of  this  formation  now  known.  It  occupies 
the  brow  of  a  hill,  underlaid  by  limestone  belonging  to  the  Niagara 
formation.  The  rock  is  here  a  rather  soft,  granular,  buff,  impure 
dolomite,  much  stained  with  iron,  doubtless  due  to  the  decomposition 
and  oxidation  of  pyrites,  originally  disseminated  through  it.  Orthis 
impressa,  /Strophodonta  demissa,  Spirifera  pinnata,  Atrypa  occi- 
dentalis,  and  A.  reticularis,  show  the  character  of  the  fauna. 

Along  the  lake  shore,  on  Whitefish  Bay,  the  formation  rises 
slightly  above  the  water  level  in  a  very  limited  exposure.  The  strata 
at  this  point  have  a  firmer  texture,  but  more  uneven  structure,  than 
at  the  previously  named  localities.  The  lines  of  deposition  and  bed- 
ding are  irregular.  Angular  cavities  of  moderate  size  are  not  unfre- 
quent,  some  of  which  are  filled  with  a  semi-fluid,  tar-like  bitumen. 
An  analysis  of  this  rock  by  Professor  Daniells  shows  it  to  have  the 
following  composition: 

Carbonate  of  lime 49.12 

Carbonate  of  magnesia 38 . 76 

Sulphate  of  lime  ..: 0-07 

Phosphate  of  lime trace. 

Sulphur trace. 

Silica 8.59 

Sesquioxides  of  iron  and  alumina   3.51 

100-05 


From  this  it  will  be  seen  to  have  much  less  silica  and  alumina  than 
the  beds  on  the  Milwaukee  river. 


400  GEOLOGY  OF  EASTERN  WISCONSIN. 

The  following  species  were  collected  at  this  point:  Orthis  im- 
pressa,  Strophodonta  demissa,  S.  perplana,  Sperifera  medialis,  S, 
pinnata,  Atrypa  reticularis,  Palceoneilo  constricta,  P.  emarginata, 
Modiomorpha  concentrica,  two  new  species  of  Gomphoceras,  Pha- 
cops  rana,  and  several  imperfect  forms  belonging  to  the  genera 
Cyathophyllum,  Lingula,  Spirifera,  Palceoneilo,  Modiomorpha  and 
Ecculio7nphalus,  and  the  plate  of  a  Placoderm  fish. 

Economic  Considerations.  The  credit  of  first  calling  attention  to 
the  hydraulic  properties  possessed  by  the  rock  of  this  formation  be- 
longs to  the  late  Dr.  I.  A.  Lapham,  who,  some  years  since,  directed 
attention  to  it  as  probably  possessing  the  property  of  hydraulicity. 
In  an  article  prepared  for  Walling's  Atlas  of  Wisconsin,  under  date 
of  July,  1874,  he  called  attention  to  the  geological  relation  existing 
between  this  rock  and  the  water-limestone  of  Louisville,  Ky.,  with  a 
suggestion  as  to  its  possessing  the  same  useful  qualities.  The  first 
investigations  upon  the  part  of  the  geological  survey  were  made  by 
the  party  under  my  charge,  between  the  5th  and  12th  of  June,  1874, 
and  specimens  were  sent  to  the  chemist  of  the  survey  for  analysis  on 
the  latter  date,  but  owing  to  the  crowded  state  of  that  department, 
analyses  were  not  received  until  the  following  year.  The  investiga- 
tions of  Dr.  Wight  upon  the  same  subject  in  the  year  1875  are  fully 
stated  in  his  Annual  Report.  The  credit  of  demonstrating  by  actual 
tests,  the  unusual  hydraulic  excellence  of  the  rock  of  this  formation, 
is  due  to  the  gentlemen  constituting  the  Milwaukee  Cement  Co.,  and 
to  Mr.  D.  J.  Whittemore,  Chief  Engineer  of  the  C.,  M.  &  St.  P.  E. 
H.  To  these  gentlemen  I  am  under  obligations  for  the  following 

CD  O  CJ 

facts,  relating  to  their  interesting  and  important  investigations:1 

The  first  series  of  experiments  of  Mr.  Whittemore  to  determine 
the  quality  of  this  rock  as  a  cement  stone,  and  the  strength  and  value 
of  the  product,  extended  continuously  over  nearly  one  year  and  a  half, 
and  embraced  about  1,500  individual  tests,  and  perhaps  an  equal  num- 
ber has  been  made  by  him  and  other  competent  gentlemen  since. 
These  experiments  were  conducted  according  to  standard  methods, 
with  excellent  apparatus,  and  appear  to  have  been  characterized  by 
impartiality  in  selection,  and  conscientious  care  in  manipulation.  The 
results  obtained  from  the  commercial  cements  with  which  comparison 
was  made  compare  very  favorably  with  those  obtained  by  other  com- 
petent experimenters  upon  the  same  products,  which  indicates  that 
the  selection  was  a  fair  one,  and  as  the  several  samples  were  subjected 
to  the  same  processes,  the  results  possess  much  more  value  than  if 

1  See  a  paper  read  before  the  Fortnightly  Club  of  Milwaukee,  November  4,1875,  by 
Don  J.  Whittemore,  of  which  the  following  is  little  more  than  an  abstract. 


HAMILTON  CEMENT  ROCK. 


401 


the  data,  with  which  comparison  is  made,  were  compiled  from  trials 
made  at  various  times,  and  under  varying  conditions  and  manipula- 
tion.1 The  Milwaukee  cement  was  prepared  by  calcination  in  cru- 
cibles with  varying  degrees  of  torrification,  and,  in  the  absence  of 
experimental  knowledge  of  the  peculiarities  of  the  rock,  it  cannot  be 
supposed  that  the  maximum  of  good  results  was  secured.  Mr.  "Whit- 
temore  expresses  the  opinion  that,  with  proper  care,  a  better  com- 
mercial article  than  the  one  used  might  be  manufactured. 

The  commercial  cements  were  obtained  as  fresh  as  possible  from 
the  stock  in  the  market,  a  selection  being  made  from  large  quantities, 
and  only  those  used,  that,  upon  trial,  were  found  to  be  of  good  qual- 
ity. To  secure  uniform  fineness,  only  that  portion  of  each  product 
was  used  that  passed  through  a  sieve  of  2^704  meshes  to  the  square 
inch. 

The  following  table  shows  the  tensile  strength  in  pounds  per  square 
inch  of  mortars  of  clear  cement,  seven  days  old,  the  last  six  in  water; 
also  of  mortars  composed  of  equal  weights  of  cement  and  sand  at  90 
days,  the  last  89  in  water: 


KIND  OF  CEMENT. 

TENSILE  STRENGTH,    IN  POUNDS 
PER  SQUARE  INCH,  OF  MORTARS 
COMPOSED  OF 

Clear  cement,  sev- 
en days  old. 

Equal  weights   of 
cement  and  sand, 
ninety  days  old. 

Commercial  Cements  — 
No.    1  

95 

77 
38 
97 
107^ 
139^ 
44 
36 
94^ 
95 
98^ 
90 

70^ 
101 
98 
96 

194 

185 

152^: 

270 
195 

204K 

2  

3  

4  

5  

7  

8  

9  

140 
182% 
280 
149 
157 
196% 
190 

202M 
290 

10  

11  

12  

13  

14  

15  

16  

In  the  above  table,  the  result  for  the  Milwaukee  cement  was  ob- 

1  Those  who  may  wish  to  compare  the  results  obtained  by  Mr.  Whittemore  with  those 
of  others  will  find  the  means  of  doing  so  in  Gen.  Q.  A.  Gilmore's  standard   work  on 
Limes.  Hydraulic  Cements  and  Mortars. 
Wis.  SUR.—  26 


402 


GEOLOGY  OF  EASTERN  WISCONSIN. 


tained  from  the  average  of  separate  tests  of  two  samples  taken  from 
widely  different  parts  of  the  outcrop  on  the  Milwaukee  river,  and  cal- 
cined, one  four,  and  the  other  three  hours,  and  from  a  mixture  of 
these  calcined  for  two  and  a  half,  three,  three  and  a  half,  four,  and  four 
and  a  half  hours,  respectively.  The  results  indicate  a  convenient  lat- 
itude in  calcination,  which  is  an  important  consideration  in  securing 
a  uniformly  reliable  commercial  product. 

To  ascertain  the  breaking  stength  of  the  cement,  rectangular  bars 
one  inch  square,  in  cross  section,  and  four  inches  long,  were  prepared, 
from  the  several  samples  tested,  in  a  precisely  similar  manner,  and  al- 
lowed to  set  under  an  end  pressure  of  32  pounds;  when  they  were 
removed  and  kept  one  day  in  air  and  ninety-nine  in  water.  They 
were  then  broken  by  resting  them  upon  supports  four  inches  apart 
and  applying  weight  gradually  at  the  center.  The  results  are  given  in 
the  following  table: 

BREAKING   STRENGTH    OF   CEMENT   MORTARS. 


KIND  OF 

CEMENT. 

WHITTEMORE. 

YARDLEY. 

Cement  2 
Sand      1 

Cement  1 
Sand      2 

Cement  2 
Sand      1 

Cement  1 
Sand      2 

Commerci 
....do... 
....do... 
....do... 
....do... 
....do... 
Milwauke 
....do... 
....do... 
....do... 
tioned) 
Milwauke 

a/1  Cement 
do.. 
do.. 
do.. 
do.. 
do.. 
3  Cement 
do.. 
do.. 
....  do.. 

No     1 

54 
59 

98K 
100 
59 
107 
119% 
120M 
11914 

138 
124 

28^ 

44^ 

44^ 
47 

44M 
56^ 
89J* 
75M 

57^ 

55 
69 

3 

4  

64 
70 

32 
33 

7  

10 

11  

62 

20 

calcined  2^  hours  .  . 
3  hours  .  .  . 
4  hours  .  . 
mixture  (before  men- 

e  cement, 

averjig'e  •  •  •  •  *  

From  the  above,  it  will  be  seen  that  the  average  breaking  strength 
of  the  Milwaukee  cement  is  16  per  cent,  higher  than  the  best  result 
obtained  from  the  six  commercial  samples  tested,  when  the  propor- 
tions were  two  of  cement  to  one  of  sand,  and  22  per  cent,  when  the 
proportions  were  one  of  cement  to  two  of  sand.  The  average  of  the 
Milwaukee  cement  exceeds  the  average  of  the  commercial  cements  by 
56  per  cent.  That  this  difference  is  not  due  to  inferiority  in  the  com- 
mercial cements  used  by  Mr.  "Whittemore  appears  from  a  comparison 
with  the  results  of  tests  made  by  Edward  Yardley,  C.  E.,  reported  in 
the  transactions  of  the  American  Society  of  Civil  Engineers  for  1872, 
and  given  in  the  table  above.  Mr.  Yardley's  specimens  were  of  sim- 


HAMILTON  CEMENT  ROCKS. 


403 


ilar  form,  composition  and  age,  but  were  made  plastic  like  mason's 
mortar,  while  Mr.  Whittemore's  were  all  made  stiff.  Making  all  due 
allowance  for  this,  it  still  appears  evident  that  Mr.  Whittemore  used 
a  superior  selection  of  commercial  cements. 

For  determining  the  crushing  strength,  cylinders  of  mortar  having 
a  base  area  of  one  square  inch,  and  a  height  of  one  inch,  were  formed 
from  the  several  cements,  and  kept  under  a  pressure  of  32  pounds 
until  set,  when  they  were  kept  in  a  dry  room  one  day,  and  then  im- 
mersed for  89  days  in  water,  when  they  were  crushed,  several  samples 
of  each  being  used.  The  following  table  gives  the  results  obtained: 

CRUSHING    STRENGTH, 
In  pounds  per  square  inch,  of  cement  mortars,  90  days  old,  the  last  89  in  ivater. 


KIND  OF  CEMENT. 

COMPOSITION  OP  MORTABS. 

** 

«*-"]""! 

O"3 
o  2 

~t^f    Ca 

fS 

btii-H 

60    - 
4j>H 

| 

3 

4  . 

•41 

|1 

£ 

o 

,—  i 

3 

CO 

.2 

exi 

-8 

CO 

3 

i—  i 

Commercial  •< 

Milwaukee    - 
Portland 

r  NO    l  

2,775 
2,200 
2,028 
3.  302 
2,983 
3,479 
4,742 
2,  767 
3,789 
3,247 
5,019 

1,930 
1,614 
1,661 
2,767 
2,k>0 
3.060 
3,475 
2,  396 
3,  156 
2,981 
3,572 

884 
794 
1,071 
1,536 
939 
1,590 
1,737 
1,596 
1,900 
2,075 
2,130 
2.340 
2,  146 
2,478 
2,497 
3,356 

299 
337 
417 
802 
742 
895 
843 
1,068 
955 
1,208 
1,192 
1,596 
1,261 
1,467 
1,479 
1,769 

128 
180 
233 
524 
472 
615 
625 
571 
586 
750 
681 
1,083 
1,127 
1,083 
1,135 
792 

1,311 
1,311 
1.721 

2,893 
2,153 
3,100 
3,205 
3,235 
3,441 
4,030 
4,  003 
5,019 
4,534 
5,028 
5,111 
5,917 

33 
33 
43 
70 
54 
77 
80 
80 
85 
100 
100 
125 
114 
125 
128 
148 

No     2  

No.    3  

No.    4  

No     5  

No     6  

No     7  

No.    8  

No.    9  
No   10  

L  No.  11  

f  A   . 

B  

3,  705 
3,887 
3,704 
5,330 

3,691 
3,321 
3,469 
4,  630 

1  C  . 

L  B  and  C  Mixture 

By  an  inspection  of  the  above  table,  it  will  be  seen  that  in  the 
strength  of  the  clear  cement,  the  commercial  articles  Nos.  7  and  11 
surpass  the  Wisconsin  product,  but  as  the  admixture  of  sand  is  in- 
creased, the  relative  superiority  of  the  latter  becomes  very  conspicu- 
ous. It  appears  that  the  larger  the  proportion  of  sand,  the  greater 
the  relative  value  of  the  Milwaukee  cement.  Since  cement  is  usually 
used  with  at  least  an  equal  quantity  of  sand,  the  columns  in  the  above 
table  that  give  the  proportions  of  1  to  1,  1  to  2,  and  1  to  3,  indicate 
the  practical  value  of  the  products  examined,  and  they  therefore  are 
combined  in  the  sixth  column  of  the  table.  The  last  column  gives  in 
a  more  convenient  form  the  value  of  the  several  cements  for  the  pro- 


404 


GEOLOGY  OF  EASTERN  WISCONSIN. 


portions  indicated,  the  two  best  commercial  cements  being  taken  as  a 
standard  of  comparison,  and  expressed  by  100.  It  will  be  observed 
that  the  average  of  the  tests  of  the  Wisconsin  product,  exceeds  the 
highest  of  the  commercial  articles  by  23  per  cent.,  and  exceeds  the 
average  of  the  eleven,  which  represent  the  relative  strength  of  the  ce- 
ment in  the  Milwaukee  market,  by  54  per  cent.  The  remarkable  im- 
ported cement,  known  as  Portland,  was  included  in  these  tests,  and  the 
results  are  given  in  the  table.  As  it  is  extensively  used  in  Europe, 
and  has  been  submitted  to  a  great  many  trials,  its  character  and  value 
are  well  known  to  engineers  and  experts,  and  it  therefore  furnishes  a 
valuable  standard  of  comparison.  Within  the  proportions  named 
above,  the  Wisconsin  cement  surpasses  the  best  of  the  commercial 
cements  almost  as  much  as  it  is  surpassed  by  this  unrivalled  artificial 
European  product. 

It  remained  to  test  the  adhesive  strength  of  this  mortar,  and  for 
this  purpose  Mr.  Whittemore  joined  common  brick  crosswise  with 
mortar  composed  of  equal  parts  of  cement  and  sand,  and  kept  them 
under  a  pressure  of  five  pounds  per  square  inch,  until  the  mortar  had 
set,  when  the  brick  were  packed  in  damp  sand  for  seventy  days,  and 
then  were  separated  by  tensile  strain,  with  the  following  results: 

Commercial  cement  No.  1 39% 


2  

59 

3  

16 

4  

.  27% 

6  

.  419^ 

7  

..  54V< 

8  

41^i 

10  

66 

11  

.  631^ 

d  cements  

..  45iX 

Average  of  three  products  of  Milwaukee  cement 75% 

English  Portland 47% 

In  many  instances,  the  result  only  shows  the  cohesive  strength  of 
the  brick,  since  after  a  strain  of  60  pounds  is  reached,  the  brick  is  of- 
ten ruptured  instead  of  the  mortar. 

Sawn  slabs  of  marble  treated  in  a  similar  manner  showed  an  adhe- 
sive strength  of  53f  pounds,  when  joined  96  days.  The  rate  of  indu- 
ration was  ascertained  by  crushing  cylinders  composed  of  equal  parts 
of  cement  and  sand,  at  the  end  of  every  five  days  up  to  ninety.  The 
following  series  indicates  the  strength,  in  pounds,  per  square  inch, 
attained,  beginning  at  the  age  of  five  days  and  ending  at  ninety:  403, 
837, 1,178,  1,519,  1,953,  2,418,  2,635,  2,759,  2,867,  2,976,  3,068,  3,162, 
3,255,  3,332,  3,410,  3,487,  3,571,  3,658. 


HAMILTON  CEMENT  ROCK.  405 

Gen.  Q.  A.  Gilmore,  U.  S.  A.,  the  highest  authority  upon  this  sub- 
ject in  this  country,  gives  as  the  average  tensile  strength  of  the  Mil- 
waukee cement,  at  the  end  of  seven  days,  64|-  pounds  to  the  square 
inch,  and  that  of  the  standard  brands  of  five  of  the  Rosendale  compa- 
nies at  47  pounds.  He  also  informs  me  that  the  commercial  product  of 
the  Milwaukee  stone,  used  under  his  direction  at  Washington  city, 
for  making  concrete,  produced  excellent  work.  Similar  testimony  is 
given  by  others  who  have  used  the  cement.  The  excellence  of  the 
product  may  therefore  be  regarded  as  established. 

Four  large  kilns,  with  a  mill  and  accessory  works,  have  been  already 
constructed  and  put  in  successful  operation.  The  extent  of  the  deposit 
is  abundantly  sufficient  for  all  anticipated  wants,  and  its  location  is 
convenient  and  accessible.  The  description  of  so  interesting  and  im- 
portant a  resource  forms  a  fitting  close  for  our  discussion  of  the  geol- 
ogy of  Eastern.  Wisconsin. 


PART  III. 


GEOLOGY 


OF 


BY  ROLAOT3  D. 


INTRODUCTION. 

The  following  report  covers  a  region  having  an  area  of  about  10,000 
square  miles,  and  is  the  result  of  something  more  than  nine  months, 
in  all,  of  field  work.  The  greater  part  of  this  was  done  in  the  seasons 
of  1874  and  1875,  my  work  during  the  other  years  of  the  existence  of 
the  survey  having  been  in  the  Lake  Superior  country,  which  will  be 
treated  of  in  a  subsequent  volume. 

The  district  now  reported  on,  including  the  central  counties  of 
Wisconsin,  is  nearly  one-fourth  larger  than  the  state  of  New  Jersey, 
whose  third  geological  survey  has  been  in  progress  from  1864  up  to 
the  present  time,  and  has  issued,  besides  numerous  annual  reports,  a 
large  volume  of  nine  hundred  pages,  and  an  atlas  of  maps.  Prof. 
Geikie,  director  .of  the  geological  survey  of  Scotland,  has  recently 
made  the  statement,  in  a  public  lecture,  that  the  average  annual 
amount  of  ground  gone  over  by  each  geologist  of  that  survey  is  about 
one  hundred  square  miles,  this  amount  of  labor  being  performed  by 
an  average  daily  walk  of  ten  to  fifteen  miles,  in  a  year  of  two  hundred 
days  in  the  field.  At  the  same  rate,  an  examination  of  the  Central 
"Wisconsin  district  would  require  over  one  hundred  years  of  continu- 
ous work.  These  statements  are  made  in  order  that  a  fair  judgment 
may  be  passed  upon  the  results  accomplished,  as  compared  with  those 
of  the  surveys  of  other  states  and  countries,  and  in  order  that  it  may 
be  understood  that  no  claim  is  made  of  having  made  an  exhaustive 
survey  of  the  district  reported  upon. 

Geological  mapping  is  accurate,  ceteris  paribus,  exactly  in  pro- 
portion as  the  geographical  maps  used  as  a  basis  are  accurate.  One 
great  advantage  enjoyed  by  the  surveys  of  Great  Britain  lies  in  the 
almost  absolute  accuracy  of  the  celebrated  Ordnance  Maps  of  that 
country,  which  are  drawn  on  a  scale  of  six  inches  to  the  mile,  and 
show  every  topographical  feature,  road,  and  house,  with  such  faithful- 
ness that  the  geologist  has  little  more  to  do  than  to  mark  upon  them 
outcrops  as  fast  as  found.  In  the  United  States,  the  only  maps  hav- 
ing any  genuine  •  claim  to  accuracy  are  those  of  the  coasts  of  the 
continent,  and  of  the  shores  of  the  great  lakes,  made  by  the  gov- 
ernment triangulation  surveys,  and  even  these  are,  for  the  most  part, 
on  too  small  a  scale  to  be  of  much  use  in  geological  mapping.  Nev- 
ertheless, in  this  regard,  we  have  in  Wisconsin  a  great  advantage  over 


410  GEOLOGY  OF  CENTRAL  WISCONSIN. 

most  of  the  older  states  of  tlie  Union,  in  the  possession  of  the  United 
States  Linear  Surveys,  which  have  divided  the  whole  state  up  into 
townships  of  thirty-six  square  miles,  and  these  again  into  sections  of  one 
square  mile  each.  Plats  of  each  towTnship  are  always  to  be  obtained, 
drawn  to  a  scale  of  two  inches  to  the  mile,  and  showing  marshes,  prai- 
ries, streams,  and  timber  land;  all  of  which  are  pretty  closely  correct 
where  crossed  by  the  section  lines,  though  elsewhere  only  roughly  ap- 
proximate. With  these  maps,  a  little  trouble  suffices  to  locate  out- 
crops with  considerable  accuracy,  and  the  task  becomes  still  easier  in 
the  case  of  those  few  counties  of  which  there  are  atlases  showing  the 
locations  of  roads  and  houses.  Notwithstanding  the  size  of  the  dis- 
trict, and  the  shortness  of  the  field  work,  it  is  believed  that  the  maps 
accompanying  this  report  will  compare  favorably  in  closeness  of  detail 
with  those  made  of  any  other  states  in  the  Union. 

The  present  report  is  the  only  comprehensive  one  ever  made  on  the 
area  included  within  the  Central  Wisconsin  district,  the  greater  part 
of  which  has,  indeed,  never  before  been  geologically  examined,  al- 
though a  number  of  recoimoissances  along  certain  lines  have  been 
made  in  former  years.  About  1847,  Dr.  Randall,  one  of  the.  corps  of 
the  United  States  survey  of  Wisconsin,  Iowa  and  Minnesota,  under 
Dr.  D.  D.  Owen,  made  a  trip  along  Black  river  from  the  falls  to  the 
Fourth  Principal  Meridian.  His  observations  occupy  two  or  three 
pages  in  Dr.  Owen's  final  report,1  and  are  accompanied  by  one  or  two 
colored  sections.  In  the  same  year,  Dr.  J.  Gr.  Norwood,  another  of  Dr. 
Owen's  corps,  made  a  canoe  trip  along  the  Wisconsin  from  its  source 
to  Sauk  City.  His  observations,  in  the  form  of  an  itinerary,  cover 
about  fifteen  pages2  of  the  same  volume,  which  includes  also  about 
twelve  pages8  by  Dr.  B.  F.  Shumard  on  the  valley  of  the  Wisconsin 
below  Portage.  In  1855,  Dr.  J.  G.  Percival,  then  state  geologist, 
spent  five  months  in  making  a  general  reconnoissance  of  the  entire 
state,  visiting  all  but  twelve  counties.  His  report  on  this  reconnois- 
sance, printed  after  his  death  in  May,  1856,  covers  about  fifty  pages, 
in  which  each  formation  is  taken  up  in  regular  order.  Whilst  this 
report  is  tinctured  somewhat  with  the  older  ideas,  and  some  of  its 
statements  have  been  since  proved  erroneous,  and  although  Dr.  Per- 
cival did  not  have  the  advantages  of  the  latest  discoveries  in  the 
science,  and  of  the  light  now  to  be  obtained  from  the  geological  reports 
of  adjacent  states,  nevertheless  his  general  summary  of  the  geology 
of  the  state,  so  far  as  my  observation  goes,  is  an  exceedingly  faithful 
one.  The  report  was  published  only  as  a  small  pamphlet,  and  has 
never  received  the  credit  it  deserved.  How  far  the  survey  under  Mr. 

1  Owen's  Geological  Survey  of  Wisconsin,  Iowa  and  Minnesota,  p.  151. 
1  Ibid,  pp.  277-293.      3  Ibid,  pp.  510-522. 


INTRODUCTION.  411 

James  Hall,  in  1S5S-1SG1,  extended  into  the  Central  Wisconsin  dis- 
trict, I  have  no  means  of  knowing,  since  no  reports  were  ever  pub- 
lished, except  that  on  the  lead  region  by  Prof.  Whitney.  The  large 
geological  chart  of  Canada  and  the  northern  United  States,  issued  by 
the  Canadian  Geological  Survey,  gives  some  quite  accurate  details 
with  regard  to  the  distribution  of  the  Lower  Silurian  formations  of 

t» 

Central  Wisconsin,  and  as  these  were  contributed  by  Mr.  Hall,  they 
would  seem  to  indicate  that  a  good  deal  of  work  was  done  by  his  sur- 
vey that  was  never  published. 

Future  surveys  will,  beyond  doubt,  make  farther  and  more  detailed 
observations  than  now  submitted,  points  now  in  doubt  will  be  cleared 
up,  and  new  generalizations,  now  unthought  of,  will  be  made. 
Amongst  those  points  that  now  appear  especially  to  need  further  in- 
vestigation, may  be  mentioned  the  detailed  structure  of  the  Archsean 
terranes  of  the  northern  part  of  the  district,  and  the  question  as  to  the 
existence  of  two  distinct  formations  within  what  is  now  called  the 
the  Potsdam  sandstone  series,  the  one  resting  upon  the  eroded  surface 
of  the  other.  The  first  of  these  can  be  fully  attained  only  by  an  ex- 
haustive traversing  of  the  unsettled  regions  on  foot,  the  location  of 
every  outcrop,  and  the  microscopic  examination  of  all  specimens. 
The  Archaean  ranges  of  the  Baraboo  valley,  too,  deserve  a  more  de- 
tailed study,  and  such  a  one  as  can  only  be  given  by  the  most  thorough 
traversing  on  foot. 

The  general  arrangement  of  this  report,  by  geological  formations, 
seems  to  be  the  only  logical  one.  A  complete  arrangement  by  coun- 
ties involves  a  great  deal  of  repetition,  and  renders  a  report  far  less 
intelligible  to  those  outside  the  state.  Nevertheless,  it  has  not  been 
thought  best  to  carry  the  geological  arrangement  too  far,  and  the  local 
details  are,  therefore,  arranged  geographically,  so  that  information 
with  regard  to  any  particular  locality  may  be  the  more  readily  found. 
Moreover,  in  giving  details  with  regard  to  the  several  Silurian  forma- 
tions, these  have  been  grouped  together,  because  in  much  of  the  dis- 
trict the  areas  occupied  by  them  are  so  interwoven  that  any  attempt 
to  give  the  details  with  regard  to  each  separately  would  result  only  in 
confusion.  It  is  a  matter  of  great  regret,  to  me  at  least,  that  the 
small  space  necessarily  assigned  to  this  report  has  rendered  it  impos- 
sible to  print  all  of  the  manuscript  prepared.  The  pages  thrown  out 
include  a  detailed  topographical  and  geological  description,  by  town- 
ships, of  most  of  the  Silurian  portion  of  the  district;  and  the  plan  of 
the  report  is  marred  by  the  omission.  An  Appendix  on  Artesian 
Wells  and  a  Chemical  Appendix,  in  which  are  tabulated,  with  addi- 
tions, the  analyses  cited  in  the  following  pages,  for  the  most  part  the 
work  of  Mr.  E.  T.  Sweet,  are  also  crowded  out. 


412  GEOLOGY  OF  CENTRAL  WISCONSIN. 

The  parenthetical  numbers  of  the  detailed  descriptions  of  this  re- 
port are  those  of  specimens  representing  the  rocks  described.  These 
specimens  will  be  distributed,  according  to  law,  to  different  institu- 
tions in  the  state,  and  will  be  much  more  valuable  for  being  cited  here. 

It  remains  to  make  acknowledgments  for  aid  received  in  the  pros- 
ecution of  the  field  work,  and  in  the  preparation  of  this  report. 

Mr.  E.  T.  Sweet,  M.  S.,  a  graduate  of  the  State  University,  aided 
me  in  the  field  work  throughout  the  season  of  1874,  and  during  much 
of  that  of  1875.  Several  of  the  towns  in  Dane  county  were  mapped 
wholly  by  him,  besides  which  he  made  many  independent  observations 
in  other  parts  of  Dane  county,  and  in  southeastern  Columbia  county 
Mr.  Sweet  also  aided  greatly  in  the  chemical  work,  having  been  thus 
employed  especially  during  the  winter  of  1875-6.  With  very  few  ex- 
ceptions all  of  the  analyses  given  in  this  report  are  Mr.  Sweet's  work, 
and  full  credit  is  given  him  here  for  them. 

The  late  James  H.  Eaton,  Professor  of  Chemistry  and  Mineralogy 
at  Beloit  College,  aided  me  in  the  field  work  during  about  two  months 
in  each  season,  his  services  being  given  for  his  expenses  only.  His 
faithful  observations,  more  especially  with  regard  to  the  Glacial  Drift, 
have  contributed  much  to  the  material  of  this  report.  It  is  no  exag- 
geration to  sav  that  in  Professor  Eaton's  death  the  state  has  lost  the 

t/ 

best  trained  and  most  accomplished,  and  at  the  same  time  one  of  the 
most  conscientious  and  painstaking  of  its  scientists. 

In  the  latter  part  of  1875,  Mr.  G.  C.  Synon,  B.  S.,  was  my  aid  in 
the  field  work.  Messrs.  Oliver  Matthews  and  ~W.  A.  Hover,  of  the 
Metallurgical  Department  of  the  State  University,  have  both  given 
aid  gratuitously  in  field  work,  and  in  making  analyses.  Analytical 
determinations  have  also  been  made  gratuitously  by  Mr.  A.  C.  Pres- 
cott,  in  the  University  laboratory.  Messrs.  J.  P.  Paine,  A.  D.  Con- 
over,  and  P.  L.  Norman  have  aided  me  in  preparing  the  cuts  and 
plates  for  this  report.  Mr.  W.  H.  Canfield,  of  Baraboo,  for  many 
years  a  surveyor  in  Sauk  county,  furnished  me  with  a  map  of  that 
county,  on  which  he  had  marked,  from  personal  observation,  the  loca- 
tion of  quartzite  outcrops,  thus  greatly  lessening  my  own  labor.  I 
should  also  add  that  Mr.  Canfield's  topographical  map  of  Sauk  county 
has  been  of  great  assistance  in  outlining  the  formations.  The  citizens 
of  the  region  generally  have  aided  me  greatly. 

This  report  has  been  nearly  all  prepared,  including  illustrations, 
and  the  examination  of  between  two  and  three  thousand  specimens, 
during  the  year  ending  June  1, 1877,  for  the  most  part  whilst  engaged 
in  teaching  several  hours  a  day;  and  the  task  has  not  been  a  light  one. 

UNIVERSITY  OF  WISCONSIN,  June  2,  1877.  •**•  D.  I. 


GEOLOGY  OF  CENTRAL  AVISCONSIN, 


CHAPTEE  I. 
SUKFACE  FEATURES  OF  CENTRAL  WISCONSIN". 

The  region  here  designated  as  Central  Wisconsin  includes  Colum- 
bia, Marquette,  Waushara,  Adams,  Juneau,  Wood,  Marathon,  Clark 
and  Jackson  counties;  all  of  Dane  and  Sauk  counties  except  the  west- 
ern tier  of  towns  in  each;  and  also  that  portion  of  Green  Lake  county 
which  lies  north  of  the  Fox  river.  The  Atlas  plates  of  Areas  D,  E,  F, 
and  H,  apply  in  part  or  wholly  to  this  region. 

RIVER  SYSTEMS  AND  GENERAL  SURFACE  SLOPES. 

Disregarding  the  small  areas  in  Clark  and  Jackson  counties  which 
drain  into  the  Chippewa  and  Trempealeau  rivers,  the  region  may  be 
said  to  include  portions  of  four  distinct  drainage  systems:  those  of 
the  Wisconsin,  Black  and  Rock  rivers,  which  flow  southward  and 
westward  to  the  Mississippi,  and  that  of  the  Fox  river,  which  flows 
northward  and  eastward  to  Lake  Michigan,  and  is  thus  tributary  to 
the  Saint  Lawrence. 

The  directions  and  areas  of  these  river  systems  are  more  or  less 
directly  influenced  by  the  rock  structure  of  the  state.  Extending  into 
Wisconsin  from  the  Upper  Peninsula  of  Michigan,  and  forming  the 
central  nucleus  of  the  northern  half  of  Wisconsin,  is  a  great  mass  of 
ancient  crystalline  rocks,  which  is  bordered  on  all  sides  by  newer  and 
undisturbed  formations,  whose  outcropping  edges,  on  the  south,  east, 
and  west,  succeed  one  another  in  concentric  bands.  The  central  crys- 
talline mass,  probably  for  the  most  part  never  covered  by  later  forma- 
tions, includes  the  highest  land  in  the  state.  It  has  a  general  slope 
to  the  southward,  reaching  its  greatest  elevation  — 1,000  feet  above 


414:  GEOLOGY  OF  CENTRAL  WISCONSIN. 

Lakes  Michigan  and  Superior  —  along  its  northern  edge,  within  thirty 
miles  of  the  latter  lake.  The  waters  which  fall  upon  it  are  shed  in 
four  different  directions:  to  the  north,  into  Lake  Superior;  to  the 
southeast,  into  Lake  Michigan;  to  the  south,  into  the  Wisconsin  — 
which  ultimately  reaches  the  Mississippi;  and  to  the  southwest  directly 
into  the  Mississippi.  The  northward  streams,  which  interlock  on  the 
'summit  of  the  divide  with  those  flowing  southeast,  south,  and  south- 
west, and  descend  in  a  distance  of  thirty  miles  nearly  a  thousand 
feet,  are  entirely  without  the  region  at  present  under  consideration. 
Of  the  streams  flowing  southwestward,  only  the  Black  river  drains 
any  considerable  portion  of  the  region,  whilst  the  southeasterly  streams 
are  mostly  outside  of  its  limits.  Some  of  the  latter  pass  directly  to 
Lake  Michigan,  whilst  others  concentrate  into  the  stream  known  as 
the  Wolf,  which,  after  leaving  the  area  of  crystalline  rocks,  takes  a 
southerly  course  until  it  meets  the  northward  flowing  Fox.  The  two, 
uniting,  pass  through  Lake  Winnebago  northward  to  Green  Bay. 
The  systems  of  the  upper  Fox  and  of  the  Rock,  though  less  immedi- 
ately under  the  influence  of  the  Archaean  watershed  of  the  north  part 
of  the  state,  are  still  directly  affected  by  the  geology  of  the  regions 
they  drain,  the  waters  of  the  upper  Fox  being  shed  to  the  east  by  the 
high  sandstone  and  drift  region  of  western  Marquette  arid  Waushara 
counties,  and  to  the  north  by  the  high  limestone  belt  which  runs 
southwestwardly  through  Green  Lake  and  Columbia,  whilst  the  tribu- 
taries of  the  Rock  river  are  shed  southeastward  by  the  same  limestone 
belt.  Although  traced  thus  directly  to  other  influences,  the  drainage 
areas  and  general  surface  slopes  of  the  southern  half  of  the  state  are 
still  in  some  degree  ultimately  attributable  to  the  position  and  shape 
of  the  Archaean  nucleus.  Whilst  the  southern  region  retains  the  gen- 
eral slope  southward  of  the  crystalline  rocks  in  the  north,  it  also  shows 
the  same  eastward  and  westward  slopes  from  a  central  north  and  south 
line.  This  seems  without  doubt  to  be  due  to  the  continuance,  beneath 
the  Paleozoic  accumulations,  of  the  Archaean  mass  with  the  same  sur- 
face structure  as  on  its  exposed  portions,  i.  e.,  a  central  north  and 
south  crest  line,  itself  sloping  southward,  from  which  there  are  east- 
ward and  westward  slants. 

Of  the  whole  area  of  the  Central  Wisconsin  district,  the  Wisconsin 
drains  about  160  townships,  including  the  eastern  part  of  Clark,  nearly 
all  of  Marathon,  a  small  part  of  eastern  Jackson,  nearly  all  of  Wood 
and  Portage,  all  of  Juneau,  nearly  all  of  Adams,  all  of  Sank,  about 
half  of  Columbia,  and  a  few  towns  in  northwestern  Dane;  the  Black 
river  drains  about  41  townships,  including  about  half  of  Clark,  nearly 
all  of  Jackson,  and  a  small  area  in  the  western  part  of  Wood;  the 


RIVER  SYSTEMS  AND  GENERAL  SURFACE  SLOPES.  415 

Fox  drains  about  49  townships,  including  the  easternmost  part  of  Mar- 
athon and  Portage,  almost  all  of  Waushara,  all  of  Marquette,  south- 
eastern Adams,  about  four  townships  in  northern  Columbia,  and  all 
of  Green  Lake  within  the  district;  and  the  Rock  drains  about  31 
townships,  including  eastern  and  southwestern  Columbia,  and  nearly 
all  of  Dane. 

Much  the  most  important  of  these  streams  is  the  Wisconsin,  which 
constitutes,  with  its  valley,  the  main  topographical  feature  of  the 
region.  The  total  length  of  this  river,  from  its  source  to  its  mouth, 
is  about  500  miles.  Rising  in  Lac  Vieux  Desert,  on  the  summit  of 
the  Archaean  watershed,  at  an  elevation  of  951  feet  above  Lake  Michi- 
gan, it  pursues  a  general  southerly  course  for  300  miles  over  the  crys- 
talline rocks,  and  then,  passing  on  to  the  sandstones  which  form  its 
bed  for  the  remainder  of  its  course,  continues  to  the  southward  for 
some  eighty  miles  more.  Turning  then  westward,  it  reaches  the 
Mississippi  within  40  miles  of  the  south  line  of  the  state,  at  an  eleva- 
tion of  only  30  feet  above  Lake  Michigan.  Like  all  the  other  streams 
which  run  to  the  south,  southeast,  and  southwest  from  the  crystalline 
rocks,  it  has  its  quite  distinct  upper  or  crystalline  rock  portion,  and 
its  lower  or  sandstone  portion.  In  the  case  of  the  Wisconsin,  how- 
ever, we  may  conveniently  regard  the  river  as  having  three  distinct 
sections:  the  first  including  all  that  part  from  the  source  to  the  last 
appearance  of  crystalline  rocks  in  the  bed  of  the  stream,  in  the  south- 
ern part  of  Wood  county;  the  second,  that  part  from  this  point  to  the 
Dalles,  on  the  south  line  of  Adams  and  Juneau  counties;  and  the 
third,  that  portion  from  the  Dalles  to  the  mouth  of  the  stream.  The 
first  of  these  divisions  is  broken  constantly  by  rapids  and  falls,  caused 
by  the  descent  south  of  the  surface  of  the  Archaean  area,  and  by  the 
obstructions  produced  by  the  inclined  ledges  of  rock  which  cross  the 
stream.  The  second  and  third  sections  are  alike  in  being  almost  en- 
tirely without  rapids  or  falls,  and  in  the  nature  of  the  bed  rock,  but 
are  separated  by  the  contracted  gorge  known  as  the  Dalles,  which, 
acting  in  some  sort  as  a  dam,  prevents  any  considerable  rise  in  the 
river  below,  the  water  above  not  unfrequently  rising  as  much  as  50 
feet  in  flood  seasons,  whilst  below  the  extreme  fluctuation  does  not 
exceed  10  feet.  The  total  lengths  of  the  Archaean,  upper  sandstone, 
and  lower  sandstone  sections  of  the  Wisconsin,  are,  respectively,  300, 
62  and  130  miles,  the  distance  through  the  Dalles  being  about  seven 
miles. 

For  a  description  of  the  course  of  the  river  more  in  detail,  we  may 
begin  with  its  entrance  into  the  district  in  the  northern  part  of  Mara- 
thon county.  From  here,  where  the  width  according  to  the  land 


416  GEOLOGY  OF  CENTRAL  WISCONSIN. 

office  plats  is  from  300  to  500  feet,  the  river  pursues  a  general  south- 
erly course  through  towns  29,  28,  27,  26,  25  and  24,  of  range  7  east, 
and  towns  24  and  23,  of  range  8  east,  in  the  southern  part  of  Portage 
county.  In  this  part  of  its  course  the  Wisconsin  flows  through  a 
densely  timbered  country,  and  has,  except  where  it  makes  rapids,  or 
passes  through  rock  gorges,  a  narrow  bottom  land,  which  varies  in 
width,  is  usually  raised  but  a  few  feet  above  water  level,  and  is  wider 
on  one  side  than  on  the  other.  Above  this  bottom,  terraces  can  often 
be  made  out,  with  surfaces  in  some  cases  one  or  two  miles  in  width. 
Above,  again,  the  country  surface  rises  steadily  to  the  dividing  ridges 
on  each  side,  never  showing  the  bluff  edges  so  characteristic  of  the 
lower  reaches  of  the  river.  Heavy  rapids  and  falls  are  made  at  Wau- 
sau  (Big  Bull  Falls),  Mosinee  (Little  Bull  Falls),  Stevens  Point,  and 
on  section  8,  town  23,  range  8  (Conant's  Kapids).  All  but  the  last 
named  of  these  are  increased  in  height  by  artificial  dams.  Two  miles 
below  the  foot  of  Conant's  Rapids,  just  after  receiving  the  Plover  river 
on  the  east,  the  Wisconsin  turns  a  right  angle  to  the  west,  and  enters 
upon  the  sparsely  timbered  sand  plains  through  which  it  flows  for  a 
hundred  miles.  At  the  bend  the  river  is  quiet,  with  high  banks  of 
sand  and  a  few  low  outcrops  of  gneiss  at  the  water's  edge.  From  the 
bend  the  course  is  westward  for  about  nine  miles;  then,  after  curving 
southward  again,  the  long  series  of  rapids  soon  begins  which,  with 
intervening  stretches  of  still  water,  extend  about  15  miles  along  the 
river  to  the  last  rapid  at  Point  Bass,  in  southern  Wood  county.  East 
of  the  river  line,  between  the  city  of  Grand  Rapids  and  Point  Bass, 
the  country  rises  gradually,  reaching  altitudes  of  100  feet  above  the 
river  at  points  ten  or  fifteen  miles  distant.  On  the  west  the  surface 
is  an  almost  level  plain,  descending  gradually  as  the  river  is  receded 
from.  At  Point  Bass  the  gneissic  rocks  disappear  beneath  the  sand- 
stones which  for  some  miles  have  formed  the  upper  portions  of  the 
river  banks,  and  now  become  in  turn  the  bed  rock;  and  the  first 
division  of  the  river's  course  ends.  The  main  tributaries  which  it 
has  received  down  to  this  point  are,  on  the  left  bank  —  the  Big  Eau 
Claire,  three  miles  below  Wausau;  the  Little  Eau  Claire,  on  the  north 
side  of  Sec.  3,  T.  25,  R.  7  E.,  just  south  of  the  north  line  of  Portage 
county;  and  the  Big  Plover,  on  Sec.  9,  T.  28,  R.  5  E.,  just  at  the 
foot  of  Conant's  Rapids;  on  the  right  bank  —  the  Placota,  or  Big  Rib, 
about  two  miles  below  Wausau ;  the  She-she-ga-ma-isk,  or  Big  Eau 
Pleine,  on  Sec.  19,  T.  26,  R.  7  E.,  Marathon  county;  and  the  Little 
Eau  Pleine,  on  Sec.  9,  T.  25,  R.  7,  in  Portage  county.  All  of  these 
streams  are  of  considerable  size,  and  drain  large  areas.  They  all 
make  much  southing  in  their  courses,  so  that  their  lengths  are  much 


RIVER  SYSTEMS  AND  GENERAL  SURFACE  SLOPES.  417 

greater  than  the  actual  distances  from  the  sources  to  the  Wisconsin 
at  the  nearest  points,  and  all  of  them  have  a  very  considerable  descent, 
making  many  rapids  and  falls  over  the  tilted  edges  of  schistose  and 
gneissic  rocks,  even  down  to  within  short  distances  of  their  junctions 
with  the  main  river.  The  streams  on  the  west  side  head  on  the  high 
country  along  the  line  of  the  Fourth  Principal  Meridian,  about  40 
miles  west  of  the  Wisconsin,  and  at  elevations  from  200  to  300  feet 
above  their  mouths;  those  on  the  east  head  on  the  divide  between  the 
Wisconsin  and  Wolf,  about  20  miles  east,  at  elevations  not  very  much 
less.  Reaching  back,  as  these  streams  do,  into  a  country  largely  tim- 
bered with,  pine,  and  having  so  large  a  descent,  they  are  of  great  value 
for  logging  and  milling  purposes. 

The  second  section  of  the  Wisconsin  river  begins  at  Point  Bass, 
with  a  width  of  from  TOO  to  900  feet.     The  next  sixty  miles  of  its 
course,  to  the  head  of  the  Dalles,  is  a  southerly  stretch,  with  a  wide 
bow  to  the  westward,  through  sand  plains,  here  and  there  timbered 
with  dwarf  oaks,  and  interspersed  with  marshes.     These  plains  stretch 
away  to  the  east  and  west  for  twenty  miles  from  the  river  bottom, 
gradually  rising  in  both  directions.     Scattered  over  them,  at  intervals 
of  one  to  ten  miles,  are  erosion  peaks  of  sandstone  from  50  to  300  feet 
in  height,  rising  precipitously  from  the  level  ground.     Some  of  these 
are  near  and  on  the  bank  of  the  river,  which  is  also  in  places  bordered 
by  low  mural  exposures  of  the  same  sandstone.     The  river  itself  is 
constantly  obstructed  by  shifting  sandbars,  resulting  from  the  ancient 
disintegration  of  the  sandstone,  which  in  the  vicinity  everywhere 
forms  the  basement  rock,  but  its  course  is  not  obstructed  by  rock 
rapids.     As  it  nears  the  southern  line  of  Adams  and  Juneau  counties, 
the  high  ground  that  limits  the  sand  plain  on  the  west,  curving  south- 
eastward, finally  reaches  the  edge  of  the  stream,  which,  by  its  south- 
easterly course  for  the  last  twenty  miles,  has  itself  approached  the  high 
ground  on  the  east.     The  two  ridges  thus  closing  in  upon  the  river 
have  caused  it  to  cut  for  itself  the  deep  and  narrow  gorge  known  as 
the  Dalles.     In  the  second  section  of  its  course,  the  Wisconsin  re- 
ceives several  important  tributaries.     Of  those  on  the  east,  the  princi- 
pal ones  are  Duck  creek  and  Ten  Mile  creek  in  the  southern  part  of 
Wood  county;  and  the  Little  and  Big  Roche  a  Cris  creeks,  both  in 
Adams  county.     The  two  former  head  in  a  large  marsh  25  miles  east 
of,  and  over  100  feet  above,  the  main  stream.     The  two  latter  head 
on  the  high  dividing  ridge  on  the  west  line  of  Waushara  county,  at 
elevations  between  150  and  200  feet  above  their  mouths.      These 
streams  do  not  pass  through  a  timbered  country,  but  have  very  valu- 
able water  powers.     Of  those  on  the  west,  two  are  large  and  irnport- 
Wis.  SUB.  — 27 


418  GEOLOGY  OF  CENTRAL  WISCONSIN. 

ant  —  the  Yellow  and  Lemonweir  rivers.  Yellow  river  heads  in 
township  25,  in  the  adjoining  corners  of  Wood,  Jackson  and  Clark 
counties,  and  runs  a  general  southerly  course  nearly  parallel  to  the 
"Wisconsin  for  over  70  miles,  the  two  gradually  approaching  one  an- 
other  and  joining  in  towship  17,  range  4  east.  The  Yellow  has  its 
Archaean  and  sandstone  sections,  the  former  exceedingly  rocky  and 
much  broken  by  rapids  and  falls,  the  latter  comparatively  sluggish 
and  without  rock  rapids.  The  upper  portions  of  the  river  extend 
into  the  pine  regions,  and  much  logging  is  done  in  times  of  high 
water.  The  water  powers  are  of  great  value.  The  Lemonweir  is  also 
a  large  stream.  Heading  in  a  timbered  region  in  the  southeast  corner 
of  Jackson  county,  it  flows  southward  for  some  distance  through 
Monroe,  and  entering  Juneau  on  the  middle  of  its  west  side,  crosses 
it  in  a  southeasterly  direction,  reaching  the  Wisconsin  in  section  24, 
township  15,  range  5  east,  having  descended  in  its  length  of  some  70 
miles  about  200  feet. 

The  "  Dalles  "  of  the  Wisconsin,  as  already  said,  is  a  narrow  pass- 
age cut  by  the  river  through  the  high  grounds  which,  after  bounding 
its  valley  on  both  sides  for  many  miles,  have  now  gradually  approached 
and  joined.  The  total  length  of  the  gorge  is  about  seven  and  one- 
half  miles.  At  the  upper  end,  about  two  miles  north  of  the  south 
line  of  Juneau  county,  the  river  narrows  suddenly  from  a  width  of 
over  one- third  of  a  mile  to  one  of  not  more  than  200  feet.  Through- 
out the  whole  length  of  the  passage  the  width  does  not  ever  much 
exceed  this,  whilst  in  one  place  it  is  only  fifty  feet.  The  water  in  the 
gorge  is  very  deep,  although  immediately  above  it  there  are  broad 
sand  flats  with  scarcely  enough  water  at  low  stages  to  float  a  canoe. 
The  perpendicular  sandstone  walls  are  from  fifteen  to  eighty  feet  in 
height,  the  country  immediately  on  top  of  them  being  about  100  feet 
above  the  river.  From  this  level,  about  midway  in  the  passage,  there 
is  a  rapid  rise  in  both  directions  to  the  summit  of  the  high  country 
on  each  side.  In  several  places  branch  gorges  deviate  from  the  main 
gorge,  returning  again  to  it;  these  are  evidently  old  river  channels 
and  are  now  closed  by  sand.  The  streams  entering  the  river  in  this 
portion  of  its  course  make  similar  cations  on  a  smaller  scale. 

At  the  foot  of  the  Dalles  the  Wisconsin  enters  upon  the  last  sec- 
tion of  its  course,  and  also  upon  the  most  remarkable  bend  in  its 
whole  length.  From  a  nearly  southerly  course  it  now  turns  almost 
due  east,  in  which  direction  it  continues  with  one  or  two  subordinate 
turns  southward  for  about  seventeen  miles,  through  low  sand  banks, 
as  far  as  Portage.  Here  it  bends  abruptly  south  again,  and, 
reaching  its  easternmost  point  at  the  mouth  of  the  Baraboo,  soon 


RIVER  SYSTEMS  AND  GENERAL  SURFACE  SLOPES.  419 

swerves  around  into  the  final  south  west  ward  stretch  to  the  Missis- 
sippi. The  cause  of  this  long  detour  to  the  east  is  sufficiently  evi- 
dent. As  the  river  leaves  the  Dalles  it  finds  lying  directly  athwart 
its  course  the  two  bold  quartzite  ranges  which  extend  east  and  west 
through  Sauk  county  for  upwards  of  twenty  miles,  and,  crossing  into 
Columbia,  finally  unite  about  eight  miles  east  of  the  county  line,  in  a 
sharp  and  bold,  eastward  projecting  point,  which  rises  400  feet  above 
the  river  bottom.  Above  Portage,  where  the  Wisconsin  forms  the 
southern  line  of  the  town  of  Lewiston,  the  ground  immediately  north, 
is  lower  than  the  water  in  the  river,  the  heads  of  Neenah  creek,  a 
tributary  of  the  Fox,  rising  within  a  short  distance  of  its  banks.  In 
times  of  high  water  the  Wisconsin  overflows  into  these  streams,  and 
thus  contributes  much  to  a  totally  different  river  system.  At  Port- 
age the  Fox,  after  flowing  south  of  west  for  twenty  miles,  approaches 
the  Wisconsin  coming  from  the  opposite  direction.  Where  the  two 
streams  are  nearest  they  are  but  two  miles  apart,  and  are  separated  by 
a  low,  sandy  plain,  the  water  in  the  Fox  being  five  feet  below  that  of 
the  Wisconsin  at  ordinary  stages.  The  greater  part  of  this  low  ground 
is  overflowed  by  the  latter  stream  in  times  of  high  water,  and  to  this 
is  chiefly  due  the  spring  rise  in  the  Fox.  After  doubling  the  eastern 
end  of  the  quartzite  ranges,  as  already  said,  the  Wisconsin  turns 
again  to  the  west,  being  forced  to  this  by  impinging  on  the  north 
side  of  a  high  belt  of  limestone  country,  which,  after  trending  south- 
west across  the  eastern  part  of  Columbia  county,  veers  gradually  to  a 
westerly  direction,  lying  to  the  south  of  the  river  along  the  rest  of  its 
course.  Soon  after  striking  this  limestone  region,  the  river  valley 
assumes  an  altogether  new  character,  which  it  retains  to  the  mouth, 
having  now  a  nearly  level,  for  the  most  part  treeless  bottom,  from 
three  to  six  miles  in  width,  ten  to  thirty  feet  in  height,  usually  more 
on  one  side  than  on  the  other,  and  bounded  on  both  sides  by  bold  and 
often  precipitous  bluffs,  100  to  350  feet  in  height,  of  sandstone  capped 
with  limestone.  Immediately  along  the  water's  edge  is  usually  a 
narrow  timbered  strip  —  rising  two  to  four  feet  above  the  river  —  which, 
is  overflowed  at  high  water.  The  line  of  bluffs  along  the  south  side 
of  the  valley  is  the  northern  edge  of  the  high  limestone  belt  just 
mentioned,  which  reaches  its  greatest  elevations  ten  to  fifteen  miles 
south  of  this  edge.  In  front  of  the  main  bluff-face,  especially  in  its 
eastern  extension,  are  frequently  to  be  seen  bold  and  high  isolated 
outliers  of  the  limestone  country.  On  the  north  bank  the  bluffs  are 
at  first  the  edges  of  similar  large  outlying  masses,  but  further  down 
they  become  more  continuous,  the  river  crossing  over  the  northwest- 
ward trending  outcrop  line  of  the  Lower  Magnesian  limestone. 


420  GEOLOGY  OF  CENTRAL  WISCONSIN. 

In  this  last  section  of  its  course  the  Wisconsin  is  much  obstructed 
by  bars  of  shifting  sand  derived  originally  from  the  erosion  of  the 
great  sandstone  formation  which  underlies  the  whole  region,  and  to 
whose  existence  the  unusual  amount  of  obstruction  of  this  kind  in 
the  river  is  due.  The  peculiar  instability  of  these  sand  bars,  and 
their  liability  to  form  and  disappear  within  a  few  hours,  renders  their 
control  very  difficult.  In  view  of  the  enormous  quantities  of  this  al- 
ready disintegrated  sand  in  the  region  drained  by  the  river  and  its 
tributaries,  many  of  which  have  their  entire  course  through  sand  dis- 
tricts, the  construction  of  a  continuous  canal  along  the  Wisconsin 
river  from  Portage  to  its  mouth,  would  appear  to  be  the  only  way 
to  utilize  the  natural  highway  from  the  lakes  to  the  Mississippi 
which  is  offered  by  this  and  the  Fox  rivers.  In  the  last  section  of  its 
course  the  Wisconsin  receives  within  the  limits  of  our  district  only 
one  stream  of  importance,  the  Baraboo,  which  enters  the  river 
near  the  easternmost  point  of  its  great  bend.  Heading  in  the  adja- 
cent corners  of  Monroe,  Yernon  and  Juneau  counties,  at  an  elevation 
of  about  400  feet  above  its  mouth,  the  Baraboo  runs  southeastward 
into  Sauk  county,  where  it  breaks  into  the  valley  between  the  two 
east  and  west  quartzite  ranges  already  alluded  to,  through  a  narrow 
gorge  in  the  northern  range.  Turning  then  eastward  it  runs  along 
the  middle  of  the  valley  between  the  two  ranges  for  about  fifteen 
miles,  and  then,  breaking  again  northward  through  the  north  range, 
follows  its  northern  side  east  to  the  Wisconsin.  The  Baraboo  is  a 
stream  of  very  considerable  size,  and  yields  a  number  of  excellent 
water  powers  in  the  valley  between  the  quartzite  ranges,  having  a 
fall  on  this  portion  of  its  course  of  seventy  feet.  The  tributaries  on 
the  south  side  of  the  Wisconsin,  in  this  section  of  its  course,  are  of 
little  importance,  owing  to  the  nearness  of  the  limestone  divide.  The 
most  noteworthy  is  Duck  creek,  which  with  its  branches  drains  a 
considerable  area  in  the  towns  of  Pacific,  Springvale  and  Courtland, 
in  Columbia  county,  cutting  a  long  way  back  into  the  divide. 


RIVER  SYSTEMS  AND  GENERAL  SURFACE  SLOPES. 


The  following  tabulation  gives  the  altitude  of  the  water  surface  of 
the  Wisconsin  at  prominent  points  from  the  source  to  the  mouth: 


DATE. 

LOCALITY. 

ALTITUDES  OF 
WATER  SURFACE 

AUTHORITY. 

Above 
Sea. 

Above 
Lake 
Mich. 

Lac  Vieux  Desert  

1532 
1204 
1119 
1104 
1065 

1049 
1001? 

814 

792 
763 
746 
715 
696 
615 

951 
623 

538| 
523) 
484 

468 
420? 

233 
211 
182 
165 
i:34 
115 
34 

Report  of  I.  A.Lapham. 
Railroad  Survey. 

Railroad  Survey. 
Railroad  Surrey. 

Railroad  Survey. 
Railroad  Survey. 

Railroad  Survey. 
Warren's  River  Survey. 
Warren's  River  Survey. 
Wan-en's  River  Survey. 
Warren's  River  Survey. 
Warren's  River  Survey. 
Wan-en's  River  Survey. 

Wausau,  above  Dam  .... 
Knowlton  jgif" 

Stevens  Point. 

Conant's  Rapids    (Sec.  8, 
T.  23,  R.  8)  
Grand    Rapids    Railroad 
Bridge  •       

Kilbourn    City    Railroad 

Aug.  27,  1867 
Sept.  9,  1867 
Sept.  17,  1867 
Sept.  27,  1867 
Oct.  12,  1867 
Nov.  6,  1867 

Portage  

Merrimac  

Sauk  City  

Spring  Green  Bridge  .... 
Muscoda  

Mouth  of  River  

The  average  velocity  of  the  river  below  Portage  is  remarkably  uni- 
form and  is  just  about  two  miles  per  hour.1  The  daily  discharge  of 
of  the  river  at  Portao-e  in  times  of  extreme  low  water  is  about 

O 

259,000,000  cubic  feet.2  The  average  fall  of  the  water  surface 
of  the  river  below  Portage  is  1^  feet  per  mile.  General  Warrren, 
from  whose  report 3  this  statement  is  taken,  very  truly  says  that  this 
rapid  fall,  were  it  not  for  the  great  amount  of  sand  in  the  river-bed, 
would  make  the  stream  a  series  of  pools  and  rock  rapids;  so  that, 
whilst  making  a  great  obstruction,  the  sand  really  gives  the  river 
what  navigability  it  possesses. 

In  subsequent  pages  are  given  a  number  of  geological  sections 
across  the  valley  of  the  Wisconsin  below  Portage.  The  profiles  of 
these  sections  are  reduced  from  the  profiles  given  in  the  atlas  of  Gen. 
Warren's  report,  and  the  geology  has  been  added  from  my  own  ob- 
servations. 

Black  river  rises  in  townships  31  and  32,  on  the  high  drift-covered 
divide  near  the  Fourth  Principal  Meridian,  at  elevations  of  over  800 
feet  above  Lake  Michigan,  runs  first  west  into  range  2,  and  then  takes 

1  Maj.  C.  R.  Sutter,  in  Chief  of  Engineer's  Report,  1867,  p.  353.       'The  same. 
3  '•  Report  on  the  Transportation  Route  along  the  Wisconsin  and  Fox  River,"  by  Gen. 
G.  K.  Warren,  U.  S.  Engineers,  Washington,  1876. 


422  GEOLOGY  OF  CENTRAL  WISCONSIN. 

a  southerly  course  through  Clark  county  as  far  as  township  24,  where  it 
begins  a  southwesterly  stretch  towards  the  Mississippi,  which  it  reaches 
in  town  17,  range  8,  on  the  boundary  line  between  Trempealeau  and 
La  Crosse  counties.  Its  total  length  is  about  150  miles,  and  total  fall 
about  750  feet.  Like  the  Wisconsin,  it  has  its  upper  or  Archaean  por- 
tion, broken  constantly  by  chutes  and  rapids  over  gneiss  and  granite, 
and  its  lower  or  sandstone  section  without  falls.  The  Archaean  sec- 
tion of  the  river  extends  to  the  town  of  Black  River  Falls,  in  town- 
ship 21,  Jackson  county,  where  the  gneissoid  granite  and  gneiss 
cause  a  long  rapid  and  disappear  finally  beneath  the  sandstones, 
which,  however,  extend  for  many  miles  northward  of  this  point  on  the 
immediate  banks  of  the  stream,  covering  the  crystalline  rocks  every- 
where except  in  the  river  bed.  Towards  its  mouth  the  valley  of 
Black  river  is  bounded  by  limestone-capped  bluffs  like  the  lower  por- 
tion of  the  valley  of  the  Wisconsin.  Like  the  Wisconsin,  again,  it 
has  its  upper  waters  in  a  pine  covered  region,  is  much  used  for  log- 
ging, and  affords  numberless  water  powers  by  its  rapid  descent  and 
frequent  rock  interruptions.  Most  of  the  branches  of  the  upper  Black 
run  over  crystalline  rocks  like  the  main  stream,  and  have  numerous 
rapids  and  falls.  Some  of  them,  however,  as  for  instance  the  East 
Fork,  reverse  the  ordinary  conditions  of  the  streams  of  the  region, 
and  have  their  upper  portions  in  sandstone  on  the  high  divide  near  the 
Meridian  in  northeastern  Jackson  and  eastern  Clark  county,  whilst 
farther  down  they  cut  into  the  crystalline  rocks,  making  the  usual 
rapids  and  falls. 

The  main  Rock  river  only  touches  the  southeastern  corner  of  our 
district  in  the  expansion  known  as  Lake  Koshkonong,  but  its  branches 
drain  nearly  all  of  Dane  and  most  of  eastern  Columbia.  These 
branches  are  everywhere  divided  from  the  tributaries  of  the  Wiscon- 
sin by  the  high  belt  of  limestone  country  already  described  as  run- 
ning southwestward  through  eastern  Columbia,  and  then  westward 
through  northern  Dane.  In  Dane  county  are  three  branches  of 
Rock  river,  draining  three  distinct  north  and  south  basins.  Central 
Dane  is  traversed  by  the  Catfish,  whose  upper  waters  expand  into 
several  large  lakes  that  lie  in  a  series  of  N".  E.  —  S.  W.  valleys  appar- 
ently of  glacial  origin.  Between  two  of  these  lies  Madison,  the  cap- 
ital city  of  the  state.  In  the  western  towns  of  Dane  are  the  heads  of 
Sugar  river,  whilst  on  the  eastern  side  the  drainage  is  into  Kosh- 
konong creek,  except  on  the  extreme  northeast,  where  it  is  eastward 
to  the  Crawfish,  as  is  also  the  case  with  the  eastern  part  of  Columbia 
county. 

The  Fox  river,  the  fourth  of  the  main  rivers  of  the  district,  heads 


RIVER  SYSTEMS  AND  GENERAL  SURFACE  SLOPES.  423 

in  the  northeastern  part  of  Columbia  county  and  the  adjoining  por- 
tions of  Green  Lake,  on  the  west  edge  of  the  high  limestone  belt 
previously  alluded  to.  Flowing  at  first  southwest  and  then  due  west 
nearly  parallel  to  the  Duck  creek  branch  of  the  Wisconsin,  it  ap- 
proaches the  latter  stream  at  Portage.  When  within  two  miles 
of  the  Wisconsin,  separated  from  it  and  from  Duck  creek  by  only  a 
low,  sandy  plain,  it  turns  abruptly  northward,  and,  with  a  sluggish 
current,  continues  on  this  course  for  twelve  miles  to  the  head  of  Lake 
Buffalo  in  the  southern  part  of  Marquette  county.  For  some  dis- 
tance below  Portage  the  river  has  been  shortened  by  cut-offs  and 
slackened  by  a  system  of  dams  and  locks.  It  has  already  been  said 
that  in  the  spring  this  portion  of  the  Fox  receives  a  large  amount  of 
water  from  the  Wisconsin,  much  of  which  reaches  it  through  a 
branch  known  as  the  Big  Slough  or  Neenah  creek,  which,  heading 
within  a  mile  of  the  Wisconsin,  in  the  town  of  Lewiston,  reaches  the 
Fox  just  south  of  the  north  line  of  Columbia  county,  in  the  town  of 
Fort  Winnebago.  At  the  head  of  Lake  Buffalo  the  Fox  begins  a  wide 
curve  which  brings  its  direction  finally  around  to  due  east.  Lake 
Buffalo  is  merely  an  expansion  of  the  river,  grown  up  with  grass  and 
wild  rice,  except  where  the  channel  crosses  it,  and  is  thirteen  and  one- 
half  miles  long  and  half  a  mile  wide.  It  runs  through  a  sand  plain, 
which  is  not  many  feet  above  its  level.  At  the  foot  of  the  lake,  near 
the  village  of  Montello,  a  dam  has  been  built  which  raises  the  lake-level 
several  feet.  From  the  foot  of  Lake  Buffalo  the  river  for  seven  miles 
has  an  irregular,  easterly  course,  with  a  somewhat  rapid  current,  to 
the  head  of  Lake  Puckawa,  which  is  eight  and  one-fourth  miles  in 
length  and  from  one  to  two  wide,  and  is  in  part  grown  up  with  reeds 
and  wild  rice.  At  the  foot  of  the  lake  there  are  wide  marshes 
through  which  the  river  leaves  on  the  north  side,  and,  after  making  a 
long,  narrow  bend  to  the  west,  begins  its  northeast  stretch  to  Lake 
Winnebago,  keeping  along  the  western  edge  of  the  northern  exten- 
sion of  the  same  limestone  ridge,  to  which  we  have  already  had  occa- 
sion so  many  times  to  refer,  until  after  it  leaves  the  district.  From 
Lake  Puckawa  to  Berlin  the  river  is  wider  and  deeper,  interrupted 
by  but  few  sandbars,  and  runs  for  a  considerable  portion  of  the  dis- 
tance between  high  banks.  The  main  tributaries  of  .the  upper  Fox 
enter  from  the  north,  and  head  in  the  high  drift-covered  region  of 
southwestern  Waushara  and  northwestern  Marquette,  at  elevations  of 
between  200  and  300  feet  above  their  mouths.  The  principal  ones 
are  the  Montello,  Mechan  and  White  rivers,  each  one  of  which 
branches  many  times  towards  its  head.  All  of  these  are  large,  clear, 
rapid  streams,  but,  running  in  sand  and  drift  bottoms,  are  not  broken 


424  GEOLOGY  OF  CENTRAL  WISCONSIN. 

by  rock  rapids.  They  are  in  many  places  utilized  for  milling  pur- 
poses. The  eastern  side  of  Waushara  county  is  drained  by  similar 
streams,  which  reach  the  Fox  through  Lake  Poygan, outside  the  lim- 
its of  the  district,  in  Fond  du  Lac  county.  The  following  figures 
with  regard  to  the  Fox  are  taken  from  the  report  of  Major  Charles 

Sutter,  already  referred  to: 

DISTANCE.      FALL. 

Miles.  Feet. 

Portage  to  head  of  Lake  Buffalo 12  7.12 

Head  of  Lake  Buffalo  to  foot  of  same 13}£  1.14 

Foot  of  Lake  Buffalo  to  head  of  Lake  Puckawa 7  5.22 

Head  of  Lake  Puckawa  to  foot  of  same  8/4  •  17 

Foot  of  Lake  Puckawa  to  Princeton 12  3.35 

Princeton  to  Berlin  bridge 203^  8 .32 


Portage  to  Berlin  bridge 73  25.32 


The  Fox  river,  at  the  foot  of  Winnebago  lock  at  Portage,  is  203.1 
feet  above  Lake  Michigan. 

The  remarkable  relations  of  the  valleys  of  the  upper  Fox  and 
lower  Wisconsin,  and  the  probable  former  drainage  southward  of 
the  whole  basin  of  the  Fox  and  Wolf  rivers,  are  alluded  to  on  a  sub- 
sequent page. 

SURFACE  RELIEFS. 

With  the  exception  of  the  sand  region  of  Juneau  and  Adams  coun- 
ties, and  portions  of  the  lower  Wisconsin  valley,  no  considerable  part  of 
the  district  can  be  designated  as  a  plain,  the  surface  being  everywhere 
roughened  by  erosion  or  heaped  up  drift.  The  extremes  of  elevation 
are,  however,  only  about  1,100  feet  apart,  being  1,263  feet  for  the  Rib 
Hills  near  Wausau,  and  134  feet  for  the  Wisconsin  river  at  Spring 
Green,  both  altitudes  being  referred  to  Lake  Michigan.  These  are, 
moreover,  at  opposite  ends  of  the  district,  the  Rib  Hill  being  itself  an 
isolated  ridge  600  feet  above  the  general  level.  For  the  most  part 
the  region  lies  between  200  and  900  feet  above  Lake  Michigan,  whilst 
the  changes  of  -level  in  any  one  vicinity,  except  in  such  districts  as 
that  of  the  Sauk  quartzite  ranges,  but  rarely  reach  300  feet. 

The  general  surface  slopes  and  the  extents  of  the  hydrographic  ba- 
sins have  already  been  indicated.  The  watersheds  need  further  re- 
mark, those  separating  the  four  great  basins  of  the  district  especially 
meriting  our  attention.  The  high  ground  which  sheds  in  different 
directions  the  waters  of  the  Wisconsin  and  the  Fox  begins  in  town- 


SURFACE  RELIEFS. 

shiD  37,  range  11  east,  at  an  elevation  of  about  900  feet,1  and  trends 
southward  through  ranges  eleven  and  ten  to  the  north  line  of  Portage 
county,  where  it  veers  into  range  nine,  which  it  follows  southward  to 
township  nineteen,  Waushara  county,  with  an  elevation  gradually 
lessening  from  600  to  500  feet.  Thus  far  the  watershed  has  been  be- 
tween the  Wisconsin  and  the  Wolf,  the  northern  branch  of  the  Fox. 
Its  upper  end,  as  far  south  as  Portage  county,  is  on  the  Archaean  rocks, 
its  height  being  augmented  by  drift,  and  its  slopes  in  both  directions 
gradual,  although  the  streams  are  constantly  broken  by  rock  rapids. 
South  of  the  north  side  of  Portage  county,  the  rock  formation  is  the 
sandstone.  Here  also  the  elevation  is  increased  by  drift  accumula- 
tions, which  occur  in  a  morainic  condition,  of  great  thickness,  and 
spread  over  a  wide  extent  of  country  east  and  west.  The  slopes  in 
both  directions  are  very  gradual.  South  of  township  nineteen  this 
divide,  which  is  now  between  the  Wisconsin  and  upper  Fox,  veers 
again  slightly  to  the  west,  and,  crossing  the  southern  end  of  Adams 
county,  is  cut  through  by  the  Wisconsin  itself  at  the  Dalles,  in  town- 
ship fourteen,  range  six,  having  here  an  elevation  of  about  400  feet. 
South  of  here  there  is  no  proper  divide  between  the  Wisconsin  and 
upper  Fox,  both  traversing  a  flat  country. 

The  watershed  between  the  Wisconsin  and  Black  rivers  follows 
nearly  the  line  of  the  Fourth  Principal  Meridian  from  township  31, 
where  it  has  an  elevation  of  about  900  feet,  to  township  20,  where  the 
elevation  is  about  4-00  feet.  As  far  south  as  township  45  this  ridge 
is  on  Archaean  rocks,  much  covered  by  drift,  whilst  further  south  the 
drift  soon  runs  out  and  the  sandstone  makes  up  the  ridge.  South  of 
township  20,  on  nearly  the  same  line,  the  high  ground  continues,  be- 
coming the  divide  between  the  Kickapoo,  Pine  and  Baraboo  branches 
of  the  Wisconsin,  and  carrying  limestone  on  the  summit. 

The  high  limestone  prairie  belt,  separating  the  systems  of  the  Rock 
and  Wisconsin,  has  already  been  several  times  spoken  of.  Beginning 
outside  the  district,  it  crosses  Green  Lake  county  in  a  S.  S.  W.  direc- 
tion, enters  Columbia  on  the  north  line  of  the  towns  of  Scott  and 
Randolph,  crosses  this  county  in  a  line  gradually  veering  to  the  west, 
and,  entering  Dane  in  the  towns  of  Dane  and  Vienna,  turns  due  west, 
in  which  direction  it  continues  to  the  Mississippi  river,  breaking 
down,  however,  on  the  line  of  Black  Earth  creek  in  the  towns  of  Mid- 
dleton  and  Cross  Plains.  On  the  west  this  divide  has  an  abrupt,  ser- 
rated face,  which  increases  in  boldness  and  height  as  followed  south- 
ward and  westward,  the  watershed  itself  reaching  altitudes  of  400  feet 

1  Hereafter  all  altitudes,  unless  otherwise  stated,  are  referred  to  Lake  Michigan,  which 
IB  taken  at  578  feet  above  the  sea. 


426  GEOLOGY  OF  CENTRAL  WISCONSIN. 

above  the  adjacent  Wisconsin.  The  eastward  slope,  on  the  other 
hand,  is,  in  Columbia  county,  very  gradual,  owing  to  the  general  de- 
scent eastward  of  the  strata.  As  the  -watershed  turns  westward  the 
direction  of  the  dip  changes  gradually  to  the  south,  its  amount  at  the 
same  time  becoming  lessened.  As  a  result  the  slopes  towards  the 
Catfish  valley  are  again  somewhat  more  abrupt,  but  never  become 
like  those  on  the  Wisconsin  side  of  the  divide. 

The  western  and  northern  face  of  this  divide,  as  indicated,  forms 
the  eastern  and  southern  side  of  the  Wisconsin  valley  continuously, 
from  the  mouth  of  the  river  to  the  easternmost  point  of  its  great 
bend.  Farther  north,  however,  the  ridge  continues  its  northeasterly 
trend,  leaving  the  Wisconsin  entirely,  and  becoming  now  the  eastern 
boundary  of  the  valley  of  the  upper  .Fox  river  as  far  as  Lake  Winne- 
bago.  This  interesting  relation,  which  is  very  instructive  as  to  the 
past  conditions  of  the  drainage  of  these  valleys,  is  finely  brought  out 
by  the  colored  Atlas  Map  of  Area  E,  on  which  the  western  edge  of 
the  main  brown-colored  (Lower  Magnesian)  area,  together  with  the 
brown  lime  (Mendota  base)  just  west  of  it,  show  the  position  of  the 
western  face  of  the  ridge  under  consideration.  The  map  will  suggest 
at  once,  what  is  in  every  way  the  truth,  that  the  valleys  of  the  upper 
Fox  and  of  the  lower  Wisconsin  are  really  one  continuous  valley,  the 
valley  of  the  upper  Wisconsin  being  an  entirely  independent  one.  As 
already  described,  the  Fox  and  Wisconsin  at  Portage  traverse  a  sandy 
plain  within  two  miles  of  one  another,  and  without  divide  of  any  kind. 
A  glance  at  the  map  will  show  that  the  Fox  makes  towards  the  Wis- 
consin exactly  as  do  other  small  tributaries  immediately  to  the 
south  —  and  from  which  there  is  also  no  divide  —  then  suddenly  turn- 
ing at  right  angles,  passes  northward  and  eastward  through  a  broad 
valley,  out  of  all  proportion  to  its  size.  The  whole  length  of  this  val- 
ley bears  testimony  to  the  former  presence  of  a  great  river.  The 
identity  of  the  two  valleys  is  still  further  shown  by  the  fact  that  they 
constitute  one  continuous  channel  of  erosion  through  the  same  geo- 
logical formations.  The  lower  Wisconsin  is  everywhere  cut  down 
through  the  Lower  Magnesian  limestone,  which  forms  horizontal 
strata  in  the  upper  parts  of  the  high  ground  on  each  side.  The  same 
formation  constitutes  the  ridge  all  along  the  southeast  side  of  the 
Fox  river,  and  moreover  was  once  spread  over  the  whole  country  north 
of  that  stream,  where  it  is  now  still  found  in  a  few  outliers  on  the 
very  highest  ground.  The  bottoms  of  both  valleys  are  composed  of 
the  Potsdam  sandstone. 

The  natural  inference  from  these  facts  is  that  Lake  Winnebago,  in- 
cluding the  whole  of  the  great  basin  of  the  Wolf,  formerly  drained 


SURFACE  RELIEFS.  427 

southward,  forming  a  continuous  river  with  the  Wisconsin  below 
Portage.  This  former  drainage  southward  has  been  suggested  by 
other  writers,  but  most  clearly  by  Geii.  G.  K.  "Warren,  in  his  recent 
report  on  the  Fox  and  Wisconsin  rivers,  in  which  he  shows  that  the 
lower  Fox,  through  which  the  entire  basin  of  the  upper  Fox  and 
Wolf  now  outlets,  is  a  modern  channel,  induced  to  form  by  a  lower 
position  of  the  continent  to  the  northward  than  it  formerly  had.  The 
real  identity  of  the  valleys  of  the  upper  Fox  and  lower  Wisconsin, 
now  shown,  seems  to  be  a  convincing  proof  of  the  theory.  Moreover, 
in  subsequent  pages  it  is  shown  that  the  upper  Wisconsin  has  also 
undergone  a  change  of  course,  having  at  one  time  passed  through  the 
Baraboo  quartzite  ranges,  in  the  gorge  now  partly  occupied  by 
Devil's  Lake,  and  reached  the  valley  of  the  lower  Wisconsin  in  the 
region  of  Sauk  Prairie,  more  than  20  miles  below  the  point  at  which 
the  Fox  and  Wisconsin  now  approach  each  other.  It  is  shown  that 
this  condition  held  until  the  Glacial  Period,  when,  tbe  gorge  through 
the  quartzite  ranges  becoming  choked  with  drift,  the  Wisconsin  was 
forced  to  find  itself  a  new  passage  around  the  eastern  point  of  those 
ranges.  But  this  passage  around  the  point  of  the  quartzite  ranges, 
and  as  far  southwest  as  the  former  junction  of  the  upper  and  lower 
Wisconsin,  is  just  as  ancient  and  as  deeply  eroded  as  the  channel 
of  the  lower  Wisconsin  itself.  It  follows  that  even  when  the  upper 
Wisconsin  had  its  former  course,  there  was  still  a  great  river  occupy- 
ing the  valley  immediately  below  Portage,  and  this  could  only  have 
come  from  the  region  of  the  Wolf  and  upper  Fox. 

Of  the  subordinate  dividing  ridges  we  need  only  mention  here  the 
quartzite  ranges  known  as  the  "  Baraboo  Bluffs;"  all  others  will  be 
described  in  the  chapters  on  local  geology.  The  Baraboo  ranges, 
however,  constitute  so  striking  a  feature  in  the  topography  of  the 
central  paloeozoic  portion  of  the  state,  and  present  so  marked  a  con- 
trast in  direction  and  outlines  to  all  other  relief-forms  south  of  the 
main  region  of  crystalline  rocks,  that  they  deserve  especial  mention. 
They  are  two  bold  east  and  west  ridges  —  the  southern  much  the  bold- 
er and  more  continuous  of  the  two — extending  through  Sank  and 
eastern  Columbia  county  for  twenty  miles,  and  lying  within  the  great 
bend  of  the  Wisconsin  river.  Their  cores  and  summits,  in  some 
places  their  entire  slopes,  are  composed  of  tilted  beds  of  quartzite, 
metamorphic  conglomerate,  and  porphyry,  whilst  their  flanks  are  for  the 
most  part  made  up  of  beds  of  horizontal  sandstone,  which,  in  lower 
places,  sometimes  surmounts  and  conceals  the  more  ancient  rocks. 
On  the  east  and  west  the  two  ranges  join,  and  thus  nearly  completely 
surround  the  lower  ground  between  them.  The  eastern  junction, 


428  GEOLOGY  OF  CENRTAL  WISCONSIN. 

caused  by  divergence  northward  of  the  southern  range,  the  northern 
retaining  its  E.  W.  direction,  is  a  bold,  sharp  point,  rising  abruptly 
400  feet  above  the  level  valley  of  the  Wisconsin.  From  this  point 
westward  the  southern  range  is  a  continuous  ridge  of  400  to  700  feet 
elevation  above  the  low  ground  on  the  south,  and  600  to  900  feet 
above  Lake  Michigan,  always  bold  on  both  sides,  often  precipitous, 
and  rising  at  top  into  long  rounded  swells,  which  not  infrequently 
show  the  bare,  purplish,  quartz  rocks.  The  wide,  level  prairie  lying 
south  of  the  middle  portion  of  this  range,  known  as  Sank  Prairie, 
makes  it  stand  out  all  the  more  boldly.  It  is  not,  however,  only  near 
by  that  this  range  is  noticeable.  It  is  seen  from  elevated  points  forty 
miles  to  the  north,  where  its  rounded  contours  distinguish  it  from  the 
horizontal  rock  elevations  seen  on  each  side  of  it.  Even  from  points 
around  Madison  —  which  has  between  it  and  the  Baraboo  Bluffs  a 
high  limestone  divide  —  by  the  aid  of  a  telescope,  their  rounded 
contours  can  be  distinguished  through  low  places  in  the  divide. 
At  their  western  ends  the  two  quartzite  ranges  are  a  number  of 
miles  apart,  but  are  joined  by  a  cross  ridge  of  nearly  the  same  alti- 
tude, which  has  probably  a  quartzite  core  throughout.  Except,  how- 
ever, over  a  large  rounded  elevation  about  midway  in  its  length,  and  in 
other  places  at  its  ends,  this  cross  ridge  shows  only  sandstone  as  the 
surface  rock.  On  the  east  the  cross  ridge  descends  rapidly  to  the 
level  of  the  Baraboo  valley.  On  the  west,  the  high  ground  descends 
only  gradually,  and  soon  showing  the  Lower  Magnesian  limestone  as 
the  surface  formation,  continues  many  miles  westward. 

A  remarkable  feature  of  all  of  the  paleozoic  portion  of  central 
Wisconsin  is  the  occurrence  of  isolated  ridges  and  peaks,  ris- 
ing from  100  to  300  feet  abruptly,  and  often  precipitously,  from 
the  low  ground  around  them,  having  an  area  on  top  of  from  a  frac- 
tion of  an  acre  to  a  square  mile,  and  composed  of  horizontally  strati- 
fied sandstone,  or  of  sandstone  capped  with  limestone.  Such  outlying 
bluffs  lie  all  along  the  face  of  the  high  limestone  country  of  Columbia 
and  Dane  counties,  and  are  generally  there  capped  by  the  same  lime- 
stone that  forms  the  elevated  land,  of  which  they  are  themselves  frag- 
ments. Others  again,  and  these  are  nearly  all  entirely  of  sandstone, 
occur  scattered  widely  over  the  central  plain  of  Adams  and  Ju- 
neau  counties,  often  covering  but  a  small  area,  and  showing  bare  rock 
from  the  base  to  the  summit,  which  not  infrequently  is  worn  into 
jagged  pinnacles  and  towers. 

The  following  tables  give  the  altitudes  of  numerous  points  through- 
out the  district,  referred  to  Lake  Michigan  as  zero.  The  railroad  ele- 
vations were  furnished  me  by  the  late  Dr.  I.  A.  Lapham,  who  ob- 


SURFACE  RELIEFS. 


429 


tained  them  directly  from  the  profiles  in  the  offices  of  the  several  com- 
panies. The  list  is  very  full,  an  altitude  being  given  for  almost  every 
section  line  crossed,  and  of  course  the  figures  have  a  high  degree  of 
accuracy.  Except  where  otherwise  stated,  the  railroad  grade  is  al- 
ways meant.  The  remaining  tables  include  a  number  of  altitudes,  de- 
termined by  the  aneroid  barometer,  which  are,  of  course,  approxima- 
tions only.  These  are  selected  from  a  list  of  many  thousand,  and 
apply  almost  wholly  to  Dane,  Columbia  and  Sauk  counties,  which 
liave  been  chosen  because  in  them  the  conditions  of  observation  were 
more  favorable,  reference  points  having  been  accessible  during  near- 
ly every  day's  work,  and  because,  also,  in  this  part  of  the  district 
the  mapping  of  the  geological  formations  required  that  the  observa- 
tions should  be  much  more  numerous,  and  consequently  more  accu- 
rate, than  elsewhere. 1  Numerous  determinations  of  altitude  were 
made  in  the  other  counties  of  the  district,  but,  on  account  of  the  dis- 
tance from  railroads  or  other  standards,  only  a  few  deserve  to  be  list- 
ed here.  The  general  altitude  of  any  portion  of  the  district  can  be 
obtained  from  the  chapters  on  local  details. 

MADISON   TO    ELEOY, 
Chicago  &  Northwestern  Railway. 


Place.  Altitude. 

East  Madison  depot 264 

Station  65, J  road  crossing 266 

"      130 273 

"      175,  (summit) 305 

"      262,  (summit) 325 

"      277,  deep  cut,  surface 355 

01  r    (  surface  Catfish  marsh 255 

315'|grade 277 

"      400,..: 285 

A  KO  i  grade 323 

458'  ]  furface 310 

"      520,  Waunakee 341 

"      570, 341 

ear?  j  surface 369 

667'igrade 395 

"      787,  Dane  depot 477 

"      900, 365 

;     -,  MO  j  surface  of  creek 233 

1002'igrade 267 

"    1039,  Lodi  depot 267 

"    1140, 319 

grade 265 

surface 255 

grade 200 

surface 175 


1200, 
1300, 


Place.  Altitude. 

( bridge. 215 

Station  1360,  •]  sur.  \Vis.riv.,  low  wat.  170 
(  sur.Wis.  riv.,  highwat.  180 

"        1380,  Merrimac  depot 215 

1460, 250 

j  grade 221 

]  surface 178 

"        IfiOO  f  ^Tade 292 

lUU'  1  top  Devil's  Nose 378 

1696,  surface 464 

"        1702 429 

1783,  Devil's  Lake,  grade  ...  386 

«        iqna   f  bridge 276 

'°8'}  surface 224 

1950,  Baraboo  depot 284 

Lyons  depot 282 

Bloom's  depot 300 

Ableman's  depot 297 

Reedsburg  depot 296 

La  Valle  depot 316 

Wqnewoc  depot 329 

Union  Center  depot 362 

Elroy  depot 360 

2  Stations  100  feet  apart,  beginning  with  Eaet 
Madison  depot  as  zero. 


1  The  aneroid  determinations  of  altitude  listed  here  are  believed  to  have  a  considera- 
ble degree  of  accuracy.  In  many  cases  the  same  point  was  visited  on  different  days, 
from  different  directions;  and  in  other  cases  a  second  barometer  was  read  half -hourly  at 
a  fixed  point,  whilst  observations  were  being  made,  tn  this  latter  way  it  seems  possi- 
ble to  attain  great  accuracy  with  the  aneroid,  especially  if  such  suitable  and  reliable  in- 
struments are  used  as  those  made  by  J.  H.  Steward,  of  London.  These  have  a  range  of 
onlv  3.000  feet,  and  show  a  variation  of  5  feet  very  distinctly. 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


ELROY    TO    MERRILLOJST. 
West   Wisconsin  Railway. 


Place.  Altitude. 

Elroy  depot 860 

Orange  depot 327 

Camp  Douglas  depot 856 

Valley  Junction  depot 354 

Lowry's  depot 389 


Place.  Altitude. 

Warren's  Mills  depot 448 

Rudd's  Mills  depot 403 

Black  River  Falls  depot 231 

Wright's  depot 353 

Green  Bay  Junction  depot 356 


WATERLOO    TO    MADISON. 
Chicago,  MilwatiJeee  &  St.  Paul  Railway. 


Place.  Altitude. 

Waterloo  depot 241 

W.  line,  Sec.  7,  T.  8,  R.  13  E 260 

W.  line,  Sec.  12,  T.  8.  R.  12  E 272 

W.  line,  Sec.  11,  T.  8,  R.  12  E 280 

Marshal  depot 286 

W.  line,  Sec.  10,  T.  8,  R.  12  E 286 

W.  line,  Sec.  4,  T.  8,  R.  12  E 278 

Deanville  depot 305 


W.  line,  Sec.  5,  T.  8 
W.  line,  Sec.  6,  T.  8 
W.  line,  Sec.  1,  T.  8 
W.  line,  Sec,  2,  T.  8 
W.  line,  Sec.  3,  T.  8 
W.  line,  Sec.  4,  T.  8 


R.  12  E 295 

R.  12  E 377 

R.  HE 315 


R.  11  E. 
R.  ll^E. 
R.  HE. 


374 
393 
369 


Place.  Altitude. 

Sun  Prairie  depot 356 

W.  line,  Sec.  8,  T.  8,  R.  11  E 349 

W.  line,  Sec.  18,  T.  8,  R.  11  E 341 

S.  line,  Sec.  13,  T.  8,  R.  10  E 353 

W:  line,  Sec.  24,  T.  8,  R.  10  E 355 

S.  line,  Sec.  23,  T.  8,  R.  10  E 322 

W.  line,  Sec.  26,  T.  8,  R.  10  E 321 

W.  line,  Sec.  34,  T.  8,  R.  10  E 277 

S.  line,  Sec.  33,  T.  8,  R.  10  E 270 

W.  line,  Sec.  5,  T.  7,  R.  10  E 286 

East  Madison  depot 268 

West  Madiwn  depot 275 

Lake  Monona  (3d  Lake) 262 

Lake  Mendota  (4th  Lake) 270 


EDGERTON  TO  BLACK  EARTH. 
Chicago,  Milwaukee  &  St.  Paul  Railway. 


Place.  Altitude. 

Edgerton  depot 242 

W.  line,  S.  E.  qr.  Sec.  4.  T.  12,  R.  4  E.  255 

W.  line,  N.  W.  qr.  Sec.  4,  T.  12,  R.  4  E.  262 

N.  line.  Sec.  5,  T.  12,  R.  4  E 268 

Mid.  W.  line,  Sec.  32,  T.  5,  R.  12  E. . .  275 

Mid.  N.  line,  Sec.  31,  T.  5,  R.  12  E. . . .  284 

E.  line,  S.  E.  qr.  Sec.  25,  T.  5,  R.  11  E. .  297 

W.  line,  S.  E.  qr.  Sec.  25,  T.  5,  R.  11  E.  285 

W.  line,  Sec.  25,  T.  5,  R.  11  E 285 

N.  line,  Sec.  26,  T.  5,  R.  11  E 272 

N.  line,  N.  E.  qr.  Sec.  23,  T.  5,  R.  11  E.  269 

W.  line,  N.  E.  qr.  Sec.  15,  T.  5,  R.  11  E.  280 

S.  line,  S.  E.  qr.  Sec.  9,  T.  5,  R.  11  E. . .  273 

Mid.  W.  line,  Sec.  9,  T.  5,  R.  11  E 279 

Stoughton  depot 279 

S.  line,  Sec.  32,  T.  6,  R.  11  E 290 

N.  line,  Sec.  32,  T.  6,  R.  11  E 294 

N.  line,  Sec.  29,  T.  6,  R.  11  E 267 

N.  line,  Sec.  20,  T.  6,  R.  11  E 267 

Mid.  W.  line,  Sec.  17,T.  6,  R.  11  E.. .  278 

N.  line.  Sec.  18,  T.  6,  R.  11  E 275 

W.  line,  Sec.  7,  T.  6,  R.  11  E 269 

S.  line,  Sec.  1,  T.  6,  R.  10  E 273 

W.  line,  Sec.  1,  T.  6,  R.  10  E 282 

W.  line,  S.  E.  qr.  Sec.  2,  T.  6,  R.  10  E. .  296 

McFarland  depot 289 

S.  line,  Sec.  34,  T.  7,  R.  10  E 292 

W.  line,  Sec.  34,  T.  7,  R.  10  E 276 


Place.  A  Ititude. 

W.  line,  N.  E.  qr.  Sec.  33,  T.  7,  R. 

10  E 265 

W.  line,  Sec.  28,  T.  7,  R.  10  E 265 

W.  line,  Sec.  29,  T.  7,  R.  10  E 265 

W.  line,  Sec.  30,  T.  7,  R.  10  E 270 

N.  line,  Sec.  36,  T.  7,  R.  9  E 267 

West  Madison  depot 275 

W. line,  N.  E.  qr.  Sec.  22,  T.  7,  R.  9  E.  291 
W.  line,  Sec.  22,  T.  7,  R/  9  E 


291 
291 
299 
326 


W.  line,  N.  E.  qr.  Sec.  21,  T.  7,  R.  9  E 

W.  line,  Sec.  16,  T.  7,  R.  9  E 

W.  line,  Sec.  20,  T.  8,  R.  9  E 

W. line,  N.  E.  qr.  Sec.  19,  T.  7,  R.  9  E.  332 

W.  line,  Sec.  18,  T.  7,  R.  9  E 340 

N.  line,  Sec.  13,  T.  1,  R.  9  E 345 

Middleton  depot 347 

W.  line,  Sec.  11,  T.  7,  R.  8  E 353 

W.  line,  S.  E.  qr.  Sec.  10,  T.  7,  R.  8  E. .  365 

W.  line,  Sec.  10,  T.  7,  R.  8  E 360 

W.  line,  Sec.  9,  T.  7,  R.  8  E 352 

W.  line,  Sec.  8,  T.  7,  R.  8  E 353 

W.  line,  Sec.  7,  T.  7,  R.  8  E &39 

W.  line,  Sec.  12,  T.  7,  R.  7  E 326 

W.  line,  Sec.  2,  T.  7,  R.  7  E 300 

Cross  Plains  depot 278 

W.  line,  Sec.  4,  T.  7,  R.  7  E 268 

Center  Sec.  31,  T.  8,  R.  7  E 250 

Black  Earth  depot 232 


SURFACE  RELIEFS. 


431 


CAMP  DOUGLAS  TO  RANDOLPH. 
Chicago,  Milwaukee  &  St.  Paul  Railway. 


Place.  Altitude. 

Camp  Douglas  depot 868 

New  Lisbon  depot 311 

Mauston  depot 806 

Kilbpurn  City  depot 816 

Lewiston  depot 231 

W.  line,  Sec.  35,  T.  13,  R.  8  E 229 

W.  line,  Sec.  6,  T.  12,  R.  9  E 243 

Portage  depot 232 

E.  line,  Sec.  6,  T.  12,  R.  9  E 233 

Near  center  Sec.  5,  T.  12,  R.  9  E 236 

Canal  crossing  N.  W.  qr.  Sec.  4,  T.  12, 

R.  9E 211 


Place.  Altitude. 

Fox  river  crossing  N.  W.  qr.  Sec.  4,  T. 

12,  R.  9  E 211 

E.  line,  Sec.  3,  T.  12,  R.  9  E 224 

E.  line,  Sec.  2,  T.  12,  R.  9  E 227 

E.  line,  Sec.  1,  T.  12,  R.  9  E 225 

E.  line,  Sec.  6,  T.  12,  R.  8  E 205 

E.  line,  Sec.  5,  T.  12,  R.  8  E 213 

E.  line,  Sec.  4,  T.  12,  R.  8  E 232 

Pardeeville  depot 237 

Cambria  depot". 284 

Randolph  depot 378 


TOMAH   TO    WAITS  ATI. 
Wisconsin  Valley  Railroad. 


Place.  Altitude. 

Tornah  depot 383 

Valley  Junction  depot 350 

N.  line,  Sec.  6,  T.  19,  R.  2  E 379 

N.  line,  Sec.  32,  T.  20,  R.  2  E  379 

Beaver  Station 379 

N.  line,  Sec.  22,  T.  20,  R.  2  E.  ......  384 

N.  line,  Sec.  12,  T.  20,  R.  2  E 386 

N.  line,  Sec.  6,  T.  20,  R.  3  E 339 

N.  line,  Sec.  31,  T.  21,  R.  3  E 391 

N.  line,  Sec.  28,  T.  21,  R.  3  E 395 

Yellow  river  crossing,  Sec.  14,  T.  21, 

R.3E 401 

W.  line,  Sec.  13,  T.  21,  R.  3  E 400 

W.  line,  Sec.  18,  T.  21,  R.  4  E 403 

W.  line,  Sec.  8,  T.  21,  R.  4  E 405 

W.  line,  Sec.  9,  T.  21,  R.  4  E 408 

W.  line,  Sec.  10,  T.  21,  R.  4  E 409 

W.  line,  Sec.  2,  T.  21,  R.  4  E 410 

W.  line,  Sec.  1,  T.  21.  R.  4  E 414 

W.  line,  Sec.  6,  T.  21,  R.  5  E 419 

W.  line,  Sec.  5,  T.  21,  R.  5  E 421 

W.  line,  Sec.  4,  T.  21,  R.  5  E 425 

W.  line,  Sec.  34,  T.  22,  R.  5  E 413 

Port  Edward  station  388 

N.  W.  corner,  Sec.  36.  T.  22,  R.  5,  E.  397 
N.  W.  corner,  Sec.  25,  T.  25,  R.  5 

E 426 

N.  line,  Sec.  24,  T.  22,  R.  5  E 433 

Centralia  depot 4.31 

Crossing  Green  Bay  R.  R 442 

N.  line,  Sec.  5,  T.  22,  R.  6  E 4-54 

N.  line,  Sec.  32,  T.  23,  R.  6  E 458 

N.  line,  Sec.  29,  T.  23,  R.  6  E 478 

N.  line,  Sec.  21,  T.  23,  R.  6  E 507 

N.  line,  Sec.  16,  T.  23,  R.  6  E 529 

Rudolph  depot,  Sec.  9,  T.  23,  R.  6 

E 562 


Place.  Altitude* 

N.  line,  Sec.  4,  T.  23,  R.  6  E 560 

N.  line,  Sec.  33,  T.  24,  R.  6  E 570 

N.  line,  Sec.  27,  T.  24,  R.  6  E 556 

N.  line,  Sec.  22,  T.  24,  R.  6  E 558 

Crossing  Mill  cr.,  S.  22,  T.  24,  R.  6  E  543 

N.  line,  Sec.  15,  T.  24,  R.  6  E 5-54 

N.  line,  Sec.  10,  T.  24,  R.  6  E 563 

Junction  City  depot 572 

N.  line,  Sec.  35,  T.  25.  R.  6  E 601 

N.  line,  Sec.  25,  T.  25,  R.  6  E 590 

N.  line,  Sec.  24,  T.  25,  R.  6  E 576 

N.  line,  Sec.  13,  T.  25,  R.  6  E 566 

N.  line,  Sec.  12,  T.  25,  R.  6  E 554 

Crossing  Little  Eau  Pleine  544 

N.  line,  Sec.  6,  T.  25,  R.  7  E 554 

N.  line,  Sec.  32,  T.  26,  R.  7  E 553 

{grade 550 

high  water. ..  538 

low  water  . . .  523 

Knowlton  depot    547 

N.  line,  Sec.  20,  T.  26,  R.  7  E 561 

N.  line,  Sec.  17,  T.  26,  R.  7  E 571 

N.  line,  Sec.  8,  T.  26,  R.  7  E 579 

N.  line,  Sec.  5,  T.  26,  R.  7  E 578 

N.  line,  Sec.  32.  T.  26,  R.  7  E 558 

N.  line,  Sec.  28,  T.  26,  R.  7  E 575 

N.  line,  Sec.  21,  T.  26,  R.  7  E 586 

N.  line,  Sec.  15,  T.  26,  R.  7  E 593 

N.  line,  Sec.  2,  T.  26,  R.  7  E 606 

N.  line,  Sec.  35,  T.  28,  R.  7  E 579 

N.  line,  Sec.  25,  T.  28,  R.  7  E 593 

N.  line,  Sec.  19,  T.  28,  R.  8  E 612 

N.  line,  Sec.  18,  T.  28,  R.  8  E 633 

N.  line,  Sec.  7,  T.  28,  R.  8  E 641 

N.  line,  Sec.  1,  T.  28,  R.  7  E 643 

Wausau  j  riv^aboVe  dam' .".'"i""  & 


623 


432 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


AMHERST  TO  MERRILLON. 

Green  Jtorj/  and  Minnesota,  Ra-ilicny. 


Place.  Altitude. 

Amherst  depot 553 

W.  line,  Sec.  18,  T.  23,  E.  10  E 539 

S.  W.  qr.  S.  W.  qr.  Sec.  13,  T.  23,  R, 


9E. 


543 


S.  W.  qr.  S.  W.  qr.  Sec.  14,  T.  23,  R.  9 

E 560 

N.  W.  qr.  Sec.  22,  T.  23,  R.  9  E 614 

S.  E.  qr.  S.  W.  qr.  Sec.  21,  T.  23,  R. 

9E 595 

N.  E.  qr.  S.  E.  qr.  Sec.  20,  T.  23,  R.  9  E.,  575 
N.  W.  qr  S.  W.  qr  Sec.  19,  T.  23,  R.  9 

E 559 

W.  line,  Sec.  19.  T.  23,  R.  9  E 528 

N.  E.  qr.  S.  W.  qr.  Sec.  24,  T.  23,  R. 

8  E  • • •  522 

N.  E.'qr.'  S.  W.'  qr'.  Sec. '  23,  T.'  23,' R'. 

8E 514 

Plover  depot 504 

N.  E.  qr.  S.  W.  qr.  Sec.  21,  T.  23,  R. 

8  E  501 

N.  E.'qr.'  N.'  W.'qr."  Sec!  29, 'f.  23,  R. 

8E 499 

W.  line,  N.  E.  qr.  Sec.  30,  T.  23,  R.  8 

E 501 

N.  W.  qr.  S.  E.  qr.  Sec.  25,  T.  23,  R. 


8E. 


497 
S.  W.  qr.  S.  E.  qr.  Sec.  26,  T.  23,  R.  8 

E  ................................  497 

N.  E.  qr.  N.  E.  qr.  Sec.  34,  T.  23,  R. 

8E  .............................  495 

N.  E.  qr.  S.  E.  qr.  sec.  33T  T.  23,  R.  8  E.,  493 
S.  E.  qr.  S.  E.  qr.  Sec.  32,  T.  23,  R.  8  E.,  488 
N.  W.  qr.  N.  E.  qr.  Sec.  5,  T.  22,  R.  7 

E  ................................  485 

S.  E.  qr.  N.  W.  qr.  Sec.  6,  T.  22,  R.  7 


E 


S.  W.  qr.  S.  W.  qr.  Sec.  1,  T. 
6E 


484 

478 

S.  line,  S.  W.  qr.  Sec.  2,  T.  22,  R.  6  E.,  470 
S.  E.  qr.  N.  W.  qr.  Sec.  10,  T.  22  R.  6 

E 470 

N.  E.  qr.  S.  W.  qr.  Sec.  9,  T.  22,  R.  6E.,  465 

Grand  Rapids  depot 448 

N.  E.  qr.  S.  W.  qr.  Sec.  7,  T.  22,  R.  6 


E.. 


435 
N.  E.  qr.  S.  W.  qr.  Sec.  12,  T.  22,  R. 

5E , 435 

S.  E.  qr.  S.  W.  qr.  Sec.  11,  T.  22,  R.  5 


E... 


436 

W.  line,  S.  E.  qr.  Sec.  15,  T.  22,  R.  5  E.,  438 
S.  W.  qr.  N.  E.  qr.  Sec.  16,  T.  22,  R. 

5E 433 

S.  E.  qr.  N.  W.  qr.  Sec.  17,  T.  22,  R. 

5E 430 

S.  E.  qr.  N.  W.  qr.  Sec.  18,  T.  22,  R.  5 

E 430 

Elm  Lake 433 

S.  E.  qr.  Sec.  15,  T.  22,  R.  4  E 433 

S.  W.  qr.  S.  W.  qr.  Sec.  16,  T.  22,  R. 


3  E 


450 


Hemlock  creek  crossing  .............  423 

N.  E.  qr.  N.  E.  Sec.  24,  T.  22,  R.  3,  E.,  417 


Place.  Altitude. 

Crossing  Yellow  river,  Dexterville  ....  417 
N.  W.  qr.  N.  E.  qr.  Sec.  21,  T.  22.  R.  3 

E 419 

S.  E.  qr.  N.  E.  qr.  Sec,  20,  T.  22,  R.  3  E  ,  439 

Haycreek  crossing,  Sec  19 410 

S.  E.  qr.  N.  E.  qr/Sec.  24,  T.  22,  R,  2  E.,  410 
N.  E.  qr.  S.  E.  qr.  Sec.  23,  T.  22,  R.  2  E.,  417 


390 


Hay  creek  crossing,  Sec.  22,  T.  22,  R.  2 

E 

Kirk  creek  crossing,  Sec.  28,  T.  22,  R.  2 

E 392 

S.  W.  qr.  N.  W.  qr.,  Sec.  28,  T.  22,  R. 

2E 395 

N.  W.  qr.  S.  W.  qr.  Sec,  29,  T.  22,  R. 

2E 390 

Scranton  depot 386 

Smoky  creek  crossing,  Sec.  25,  T.  22, 

R.I  E 382 

S.  E.  qr.  N.  W.  qr.  Sec.  35,  T.  22,  R.  1 

E 385 

.  395 


W.  line,  Sec.  28,  T.  22,  R.  1  E  ....... 

Creek  crossing,  S.  E.  qr.  Sec.  29,  T.  22, 

R.  1  E  ...........................  404 

N.  W.  qr.  S.  E.  qr.  Sec.  30,  T.  22,  R. 

IE  ..............................  382 

Creek  crossing,  N.  W.  qr.  Sec.  25,  T. 

22,R.1W  .......................  393 

1-5  mile  west  ......................  416 

S.  W.  qr.  S.  W.  qr.  Sec.  23.  T.  22,  R. 

1  W  ....................  ........  426 

Near  center,  Sec.  22,  T.  22.  R.  1  W.  .  .  402 
S.  W.  qr.  N.  E.  qr.  See.  21,  T.  22,  R. 

1  W  ............................  400 

S.  W.  qr.  N.  E.  qr.  Sec.  20,  T.  22,  R. 

1  W  .............................  393 

N.  W.  qr.  N.  E.  qr.  Sec.  19,  T.  22,  R. 

1  W  .............................  384 

N.  line,  S.  E.  qr.  Sec.  24,  T.  22,  R.  2  W.,  384 
S.  E.  qr.  S.  E.  qr.  Sec.  14,  T.  22,  R.  2 

W...:  .........................  364 

N.  E.  qr.  S.  E.  qr.  Sec.  15,  T.  22,  R.  2 

W..     ..........................  362 

S.  E.  qr.  N.  E.  qr.  Sec.  16,  T.  22,  R.  2 

W  ..............................  347 

W.  line,  N.  W.  qr.  Sec.  16,  T.  22,  R.  2 

W  ........    ....................  335 

W.  line,  N.  W.  qr.  Sec.  17,  T.  22,  R.  2 

W  ..............................  333 

S.  W.  qr.  N.  W.  qr.  Sec.  18,  T.  22,  R. 

2W  .............................  384 

S.  E.  qr.  S.  E.  qr.  Sec.  12,  T.  22,  R.  3 

W  ..............................  323 

S.line,N.E.qr.Sec.ll,T.22,R.3,W.,  338 

Crossing  Black  river,  j  g*^  ;  ;       ;  fgf 

N.E.qr.N.E.qr.Sec.4,T.22,R.3W.,  338 
S.E.qr.S.E.qr.Sec.22,T.23,R.3W.,  350 
S.E.  qr.  S.  W.  qr.  Sec.  20,  T.23,  R.  3 
W  ..............................  388 


Hall  s  r>rpplr    rmSsino-  \  g^de  .......    344 

5ing'  \  surface  ......  328 

Merrilon  depot  ......  ..........  .  ----  356 


SURFACE  RELIEFS. 


433 


PORTAGE  TO  STEVENS  POINT. 


Wisconsin  Ceiitotil  RaAl'road  Surveys. 


Place. 
Porta0^  depot  

Alti 

tide. 
232 
227 
223 
220 
276 
225 
228 
227 

230 
218 
218 
225 
344 
344 
338 
344 
401 
4:34 
499 
550 
544 
534 
516 
514 

Place. 
N  line,  Sec  18  T  18  R  8  E 

Altitude. 
594. 

N.  line,  S.  E.  qr.  Sec.  23,  T.  13,  R 
N.  line,  Sec   21,  T  13  R  9E.. 

9E. 

S.  line,  Sec.    4,  T.  18,  R.  8  E.  . 

524 

N.  line,  Sec  28,  T  19  R  8  E 

519 

N  line,  Sec  16,  T.  13,  R  9  E  .  . 

Hancock  depot  

513 

X.  line,  Sec.    9,  T.  13,  R.  9E.. 
N  line,  Sec     4  T  13  R  9E.. 

N.  line,  Sec.  10,  T.  19,  R.  8  E.  .  . 

520 

N.  line,  Sec.  11  T  19  R  8  E 

529 

N  line,  Sec  32,  T   14,  R  9  E  .  . 

N.  line,  3ec.    2,  T  19  R  8  E 

538 

N.  line,  Sec.  29,  T  14,  R.  9  E.  . 

N.  line,  Sec.  35,  T.  20,  R  8  E. 

..     542 

N.  line,  Sec  26  T  20  R  8  E 

561 

N.  line,  Sec.  17,    -\  g^gng 

N.  line,  Sec.  24,  T  20  R  8  E 

.     561 

W  line,  Sec     8  T  14,  R.  9  E.  . 

N.  line,  Sec.  13,  T  20  R  8  E.    . 

532 

S    line    Sec  30  T  15  R  9E.. 

Plainfield  depot  

532 

N  line   Sec  30  T  15  R  9E.. 

N.  line,  Sec     1  T  20  R  8  E 

.  .     518 

N.  line,  S.  E.  qr.  Sec.  19,  T.  15,  R. 
N  line    Sec     4  T  15  R  8  E.. 

9E. 

N.  line,  Sec.  36,  T.  21,  R.  8  E.  .  . 
N  line    Sec  25  T  21   R  8  E 

....  527 
524 

N  line    Sec  33  T  16  R  8E.. 

N  line,  Sec  12  T  21  R  8  E 

495 

N.  line,  S.  E.  qr.  Sec.  21,  T.  16,  R. 
"NT.  line,  S.  E.  qr.  Sec.  16,  T.  16,  R. 
:N.  line,  S.  E.  qr.  Sec.  32,  T.  17.  R. 
N'.  line,  Sec.  32,  T.  17,  R.  8E.. 
N  line    Sec  19  T  17  R  8E... 

8E. 
8E. 
8E. 

N.  line,  Sec.    1,  T.  21,  R.  8  E.  .  . 

494 

N.  line,  Sec.  36,  T.  22,  R.  8  E.  .  . 

493 

N.  line,  Sec.  25,  T.  22,  R  8  E.  .  . 

492 

N.  line,  Sec.  24,  T.  22,  R  8  E.  .  . 

494 

8E.  485 
.  .  .     496 

N.  W.  corner  Sec.  18,  T.  17,  R.  8  E.  . 
N  line    Sec  17  T  17  R  7E  

W.  line,  N.W.  qr.  Sec.  12,  T.  2^2,  R 
N  line   Sec  2  T  22  R  8  E  

N  line,  Sec  36,  T.  18,  R  7  E.  .  . 

1ST  line   Sec  25  T  18  R  7  E  .  .  . 

Plover  depot  

496 

Middle  E.  line.  Sec.  24.  T.  18.  R. 

7E, 

Stevens  Point  deoot.  . 

.  508 

STEVENS  POINT  TO  THE  NORTH  LINE  OF  TOWNSHIP  29. 
Wisconsin  Central  Railway. 


Place.  Altitude. 

Stevens  Point  depot  .................  508 

Cutting  N.  E.  qr.  Sec.  (  grade  .........  517 

31,  T.  24,  R.  8  E.  .  (  surface  .......  548 

N.  W.  corner  Sec.  31,  T.  24,  R.  8  E.  .  511 
N.  line,  S.  W.  qr.  Sec.  25,  T.  24,  R.  7  E.  511 
S.  line,  S.  E.  qr.  Sec.  23,  T.  24,  R.  7  E.  .  513 
W.  line,  Sec.  15,  T.  24,  R.  7  E  .......  550 

W.  line,  Sec.  16,  T.  24,  R.  7  E  .......  526 

"W.  line,  Sec.    8,  T.  24,  R.  7  E  ......     519 

W.  line,  Sec.    7,  T.  24,  R.  7  E  .......  522 

W.  line,  Sec,    1.  T.  24,  R.  6  E  .......  543 

W.  line,  Sec.    2,  T.  24,  R.  6  E  .......  563 

W.  line,  Sec.    3,  T.  24,  R.  6  E  .......  587 

W.  line,  Sec.  4,  T.  24,  R.  6  E 
"W.  line,  Sec.  32,  T.  25,  R.  6  E 
W.  line,  Sec.  31,  T.  25,  R.  6  E 
W.  line,  Sec.  36,  T.  25,  R.  5  E 
W.  line,  Sec.  35,  T.  35,  R.  5  E 
W.  line,  Sec.  34,  T.  25,  R.  5  E 
W.  line,  Sec.  28,  T.  25,  R.  5  E 
W.  line,  Sec.  29,  T.  25,  R.  5  E 
W.  line,  Sec.  30,  T.  25,  R.  5  E 
W.  line,  Sec.  25,  T.  25,  R.  4  E 
W.  line,  Sec.  26,  T.  25,  R.  4  E 


606 
615 
615 
612 
623 
608 
588 
588 
583 
631 
639 


Place.                                       Altitude. 
W.  line,  Sec.  22,  T.  25,  R.  4  E 650 

W  linp  Spr-  91  T  91  Tf  4-P  $  grade..  658 
W .  line,  bee.  U,  i:»,  JS.  4&  j  gurface  665 

W.  line,  Sec.  20,  T.  25,  R.  4  E 626 

W.  line,  Sec.  19,  T.  25,  R.  4  E 658 

W.  line,  Sec.  13,  T.  25,  R.  3  E 678 

W.  line,  Sec.  14,  T.  25,  R.  3  E 670 

W.  line,  Sec.  15,  T.  25,  R.  3  E 680 

W.  line,  Sec.    9,  T.  25,  R.  3  E 693 

W.  line,  Sec.    8,  T.  25,  R.  3  E 716 

N.  W.  corner  Sec.  6,  T.  25,  R.  3  E. ...  699 

N.  line,  Sec.  26,  T.  26,  R.  2  E 721 

N.  line,  Sec.  22,  T.  26,  R.  2  E 735 

N.  line,  Sec.  16,  T.  26,  R.  2  E 721 

N.  line,  Sec.    8,  T.  26,  R.  2  E 731 

W.  line,  S.  W.  qr.  Sec.  18,  T.  28,  R.  2  E  768 
W.  line,  S.  W.  qr.  Sec.  7,  T.  28,  R.  2  E.  789 
E.  line,  S.  E.  qr.  Sec.  1,  T.  28,  R.  1  E  .  821 

N.  line,  Sec.  35,  T.  29,  R.  1  E 830 

N.  line,  Sec.  25,  T.  29,  R.  1  E 847 

N.  line,  Sec.  24,  T.  29,  R.  1  E 842 

N.  line,  Sec.  13,  T.  29,  R.  1  E 838 

N.  line,  Sec.  12,  T.  29,  R.  1  E 866 

N.  line,  Sec.    1,  T.  29,  R.  1  E 855 


Wis.  SUR.  — ! 


4:36 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


BAKOMETKICAL  ALTITUDES  —  continued. 


Fitchbnrg.    T.  6,  R.  9  E.  —  (con.) 

Cross  roads,  E.  hf.  Sec.  19 470 

Mid.  E.  line  Sec.  19    440 

S.  W.  cor.  Sec.  19 490 

Mid.  S.  line  Sec.  19 460 

Center  Sec.  20 430 

Center  Sec.  21 550 

School  House,  E.  hf.  Sec.  21 470 

Road,  S.  E.  qr.  S.  E.  qr.  Sec.  21.. ..  455 

Mid.  E.  hf.  Sec.  22 425 

Creek  crossing,  S.  E.  qr.  Sec.  24.  ...  316 

Mid.  S.  line  S.  E.  qr.  Sec.  24 340 

S.  E.  qr.  S.  E.  qr.  Sec.  25 409 

Mid.  W.  line  N.  W.  qr.  Sec.  26. ...  460 

Center  Sec.  27 421 

Center  Sec.  28 367 

Mid.  E.  hf.  Sec.  29 480 

Mid.  W.  hf.  Sec.  29 450 

Center  Sec.  30 420 

Mid.  W.  line  Sec.  30 480 

Mid.  W.  line  Sec.  31 465 

Oak  Hall,  center  Sec.  33 354 

Mid.  E.  line  Sec.  33 353 

Center  Sec.  34 345 

Mid.  W.  hf .  Sec.  36 407 

Center  Sec.  36 385 

Dunn.    T.  6,  R.  10  E. 
Road  forks,  E.  line  N.  E.  qr.  Sec.  1.  280 
Road  forks,  W.  line  N.  W.  qr.  Sec.  1  290 

Mid.  N.  hf.  Sec.  2 / 320 

Creek  crossing,   center  N.  W.   qr. 

Sec.  7 255 

Mid.  E.  hf.  Sec.  16 315 

Mid.  W.  hf.  Sec.  16 315 

Mid.  W.  line  Sec.  16 300 

Creek  crossing,  S.  line  S.  W.  qr.  Sec. 

16 270 

Center  Sec.  17 265 

Center  S.  line  Sec.  17 290 

Creek  crossing,  N.  W.  qr.  Sec.  18. .  255 

S.  W.  cor.  Sec.  18 270 

Mid.  E.  line  Sec.  19 330 

Stream  crossing,  near  center  Sec.  20  316 

S.  W.  cor.  Sec.  20 340 

Center  Sec.  21 325 

Center  S.  line  Sec.  21 325 

Center  S.  line  S.  W.  qr.  Sec.  21 ....  360 

S.  E.  cor.  Sec.  21 293 

Mid.  E.  line  S.  E.  qr.  Sec.  21 354 

Mid.  S.  line  Sec.  22 285 

S.  W.  cor.  Sec.  23 298 

Mid.  S.  line  Sec.  25 275 

Mid.  E.  line  Sec.  31  . .   360 

Mid.  S.  line  Sec.  33 315 

Mid.  S.  line  S.  E.  qr.  Sec.  33 275 

Mid.  S.  line  S.  W.  qr.  Sec.  34 275 

Mid.  S.  line  S.  W.  qr.  Sec.  35 295 

Pleasant  Springs.    T.  6.  R.  11  E. 
Bend  in  road,  S.  line  S.  W.  qr.  Sec.  2  350 

Mid.  S.  line  Sec.  3 350 

S.  W.  cor.  Sec.  3 335 

Mid.  W.  line  Sec.  3 400 

N.  W.  cor.  Sec.  3 400 

Mid.  S.  line  Sec.  4 380 

Mid.  W.  hf.  Sec.  4 325 


Pleasant  Springs.  T.  6.  R.  11  E.— (con.) 

Mid.  S.  line  S.  E.  qr.  Sec.  6 340 

Center  S.  line  Sec.  8 270 

S.  E.  cor.  Sec.  8 285 

S.  E.  cor.  Sec.  9 329 

Mid.  E.  line  Sec.  9 340 

Quarry,  N.  E.  qr.  N.  E.  qr.  See.  10.  410 

Mid.  N.  hf.  Sec.  11 280 

Center  S.  E.  qr.  Sec.  11 320 

Mid.  N.  hf.  Sec.  13. 320 

Mid.  E.  line,  S.  E.  qr.  Sec.  13 325 

S.  E.  cor.  Sec.  13 370 

Mid.  W.  line  N.  W.  qr.  Sec.  13. ..  300 

S.  W.  cor.  Sec.  14 320 

Mid.  S.  line  See.  15 290 

Mid.  W.  line  S.  W.  qr.  Sec.  15  ...  260 

Mid.  S.  line  Sec.  17 265 

Center  Sec.  22 268 

Mid.  S.  line  Sec.  22 340 

S.  E.  cor.  Sec.  24 400 

Mid.  E.  line  Sec.  25 380 

Mid.  W.  line  Sec.  31 305 

Center  Sec.  31 300 

Center  Sec.  32 280 

Mid.  W.  hf.  Sec.  34 308 

Mid.  N.  hf.  Sec.  34 260 

Mid.  W.  hf .  Sec.  35 340 

Mid.  E.  line  Sec.  36 310 

S.  E.  cor.  Sec.  36 350 

Christiana.    T.  6.  R.  12  E. 

Mid.  W.  line  Sec.  2 290 

Mid.  E.  hf .  Sec.  3 280 

N.  W.  cor.  Sec.  6 315 

Mid.  S.  line  S.  E.  qr.  Sec.  6 285 

Stream  crossing,  N.  hf.  Sec.  7 275 

Mid.  S.  hf.  Sec.  7 330 

Mid.  E.  hf .  Sec.  10 320 

Mid.  W.  hf.  Sec.  11 280 

Mid.  E.  line  Sec.  11 260 

Mid.  N.  hf.  Sec.  12 230 

Mid.  E.  hf .  Sec.  12 230 

Stream  crossing,  mid.  W.  line  Sec.14  290 

S.  E.  cor.  Sec.  15 325 

Mid.  S.  line  Sec.  15 350 

Mid.  E.  line  N.  E.  qr.  Sec.  15 315 

Mid.  S.  line  Sec.  16 385 

S.  W.  cor.  Sec.  16 400 

Mid.  S.  line  S.  E.  qr.  Sec.  17 410 

S.  W.  cor.  Sec.  17 355 

Center  Sec.  18 315 

Mid.  S.  line  Sec.  18 340 

Stream,  E.  line  S.  E.  qr.  Sec.  21.. ..  315 

Mid.  E.  line  S.  E.  qr.  Sec.  22 360 

S.  E.  cor.  Sec,  22 320 

Cross-roads,  S.  line  S.  E.  qr.  Sec.  23.  310 

N.  W.  cor.  Sec.  27 375 

Cross  Plains.    T.  7,  R.  7  E. 

Mid.  E.  line  Sec.  1 400 

Cross  Plains  depot,  Sec.  3 274 

Top  of  bluff,  N.  lineN.  W.  qr.  Sec.  3.  420 

Mid.  S.  line  Sec.  3 400 

Mid.  E.  line  N.  E.  qr.  Sec.  7 345 

Center  Sec.  10 325 

Center  S.  E.  qr.  Sec.  10 330 

Mid.  E.  line  Sec.  11 326 


SURFACE  RELIEFS. 


437 


BAROMETRICAL  ALTITUDES  —  continued. 


Cross  Plains.    T.  7,  R.  7  E.  —  (con.) 

Mid.  E.  line  S.  E.  qr.  Sec.  12 339 

Mid.  W.  line  N.  W.  cor.  Sec.  15...  480 

Center  S.  W.  qr.  Sec.  15 490 

Mid.  S.  line  S.  W.  qr.  Sec.  15 400 

Mid.  N.  hf.  Sec.  17 325 

Mid.  W.  line  N.  W.  qr.  Sec.  17. ...  340 

Mid.  E.  line  Sec.  19 550 

Mid.  E.  line  N.  E.  qr.  Sec.  19 480 

Mid.  E.  line  S.  E.  qr.  Sec.  19 595 

S.  E.  cor.  Sec.  19 570 

Mid.  S.  line  Sec.  20 495 

S.  E.  cor.  Sec.  21 490 

Mid.  W.  hf.  Sec.  22 390 

Mid.  W.  line  S.  W.  qr.  Sec.  27 405 

Stream,  center  S.  E.  qr.  Sec.  33 405 

Middleton.    T.  7,  R.  8  E. 

Road  forks,  E.  hf.  Sec.  2 367 

Mid.  W.  line  Sec.  2 367 

Center  Sec.  3 367 

Center  Sec.  4 447 

Mid.  W.  line  Sec.  4 407 

Mid.  E.  hf.  Sec.  5 421 

Mid.  W.  hf .  Sec.  51 507 

Mid.  E.  hf .  Sec.  6 547 

Mid.  W.  hf .  Sec.  6 527 

Mid.  W.  line  S.  W.  qr.  Sec.  7 339 

Center  Sec.  9 352 

Center  Sec.  10 365 

Stream  crossing1,  N.  hf .  Sec.  11 357 

Road  forks.  E.  hf .  Sec.  12 320 

Mid.  E.  line  Sec.  13 345 

Mid.  S.  line  Sec.  13 415 

Mid.  S.  line  Sec.  14 410 

S.  W.  cor  Sec.  14 390 

Mid.  S.  line  S.  E.  qr.  Sec.  15 380 

Mid.  W.  line  Sec.  16 553 

Mid.  W.  hf.  Sec.  17 453 

Mid.  S.  line  Sec.  17 518 

Center  S.  W.  qr.  Sec.  17 555 

Mid.  S.  line  S.  W.  qr.  Sec.  17 518 

Mid.  E.  line  N.  E.  qr.  Sec.  18 353 

Center  N.  E.  qr.  Sec.  18 428 

20  rods  south  of  last 541 

Mid.  N.  hf.  Sec.  20 540 

Mid.  S.  hf.  Sec.  20 503 

b  E.  cor.  Sec.  20 508 

Mid.  S.  line  Sec.  21 538 

Mid.  S.  line  S.  W.  qr.  Sec.  22 508 

Mid.  S.  line  S.  E.  qr.  Sec.  22 478 

S  E.  cor.  sec.  23 450 

Mid.  S.  line  Sec.  24 425 

Mid.  S.  line  Sec.  27 498 

S.  W.  cor.  Sec.  27 550 

S.  W.  cor.  Sec.  28 495 

Mid.  S.  line  Sec.  29 480 

S.  W.  cor.  Sec.  29 535 

Mid.  E.  line  Sec.  31 540 

Mid.  E.  line  N.  E.  qr.  Sec.  31 600 

S.  W.  cor.  Sec.  32 560 

Center  Sec.  34 508 

Mid.  S.  line  Sec.  34 478 

S.  E.  cor.  Sec.  34 558 

Mid.  S.  line  S.  W.  qr.  Sec.  35 513 

Mid.  S.  line  S.  E.  qr.  Sec.  35 433 


Middleton.    T.  7,  R.  8  E.  —  (con.) 

Center  Sec.  35 448 

Mid.  E.  line  S.  E.  qr.  Sec.  35 530 

Mid.  E.  line  Sec.  35 428 

Center  Sec.  36 488 

Mid.  E.  hf .  Sec.  36 458 

Madison.    T.  7,  R.  9  E. 

Lake  Mendota 270 

Capitol  Hill,  S.  W.  cor.  Sec.  13  ....  348 
University  Hill,  S.  W.  cor.  Sec.  14  .  372 

Railroad,  S.  line  Sec.  16 260 

Mid.  S.  line  Sec.  18 332 

Mid.  S.  line  S.  W.  qr.  Sec.  19 450 

Mid.  S.  line  Sec.  19 415 

S.  E.  cor.  Sec.  19 400 

Mid.  S.  line  S.  W.  qr.  Sec.  20 360 

Mid.  S.  line  S.  E.  qr.  Sec.  20 435 

Mid.  S.  line  S.  W.  qr.  Sec.  21 415 

Center  N.  W.  qr.  S.  E.  qr.  Sec.  21  .  390 

Lake  Monona 262 

Road,  mid.  S.  line  Sec.  26 315 

Center  S.  W.  qr.  Sec.  28 295 

S.  line  S.  W.  qr.  S.  W.  qr.  Sec.  28.  360 

Mid.  W.  line  Sec.  31 478 

Center  Sec.  31 458 

Mid.  E.  line  Sec.  31 448 

Mid.  W.  hf.  of  E.  hf.  of  Sec.  32. ...  438 

Mid.  S.  hf.  Sec.  33 320 

Mid.  E.  line  Sec,  34 290 

Center  Sec.  35 300 

Blooming  Grove.    T.  7,  R.  10  E. 

Mid.  N.  line  N.  W.  qr.  Sec.  3 338 

Mid.  E.  hf .  Sec.  4 315 

Mid.  W.  hf.  Sec.  9 325 

Center  Sec.  9 310 

Mid.  W.  hf.  E.  hf.  Sec.  10 390 

Mid.  W.  hf.  W.  hf.  Sec.  11 410 

Mid.  W.  hf.  Sec.  11 455 

Mid.  W.  hf.  Sec.  12 400 

%  mile  W.  of  center  of  Sec.  12 330 

Center  1ST.  E.  qr.  Sec.  15 340 

Center  S.  line  S.  E.  qr.  Sec.  15 290 

S.  W.  corner  Sec.  15 310 

Mid.  W.  hf .  Sec.  16 310 

Mid.  W.  hf.  E.  hf.  Sec.  20 320 

Mid.  W.  line  Sec.  21 330 

Center  S.  W.  qr.  Sec.  21 290 

Center  S.  E.  qr.  S.  E.  qr.  Sec.  21 ...  270 

N.  W.  cor.  Sec.  22 310 

Center  S.  E.  qr.  Sec.  22 290 

Mid.  W.  line  Sec.  26 290 

%  mile  E.  of  W.  line  Sec.  27  ....     280 

Mid.  N.  line  Sec.  30 300 

Mid.  W.  line  N.  E.  qr.  Sec.  30  ....  310 
One-sixth  mile  E.  N.  W.  cor.  Sec.  35.  350 
Center  Sec.  35 340 

Cottage  Grove.    T.  7,  R.  11  E. 

Mid.  N.  line  Sec  1  320 

Mid.  E.  line  Sec.  1 350 

Center  N.  W.  qr.  Sec.  1 295 

Mid.  W.  line  S.  W.  qr.  Sec.  2 365 

Center  S.  W.  qr.  N.  W.  qr.  Sec.  2  .  275 

Mid.  W.  line  S.  E.  qr.  Sec.  3 360 

Mid.  W.  line  N.  E.  qr.  Sec.  4 320 

Mid.W.  line  S.W.  qr.  S.W.  qr.  Sec.  55  35 


4:36 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


BAKOMETTUCAL  ALTITUDES  —  continued. 


Fitchburg.    T.  6,  R.  9  E.  —  (con.) 

Cross  roads,  E.  hf.  Sec.  19 470 

Mid.  E.  line  Sec.  19    440 

S.  W.  cor.  Sec.  19 490 

Mid.  S.  line  Sec.  19 460 

Center  Sec.  20 430 

Center  Sec.  21 550 

School  House,  E.  hf.  Sec.  21 470 

Road,  S.  E.  qr.  S.  E.  qr.  Sec.  21.. ..  455 

Mid.  E.  hf.  Sec.  22 425 

Creek  crossing,  S.  E.  qr.  Sec.  24.  ...  316 

Mid.  S.  line  S.  E.  qr.  Sec.  24 340 

S.  E.  qr.  S.  E.  qr.  Sec.  25 409 

Mid.  W.  line  N.  W.  qr.  Sec.  26. ...  460 

Center  Sec.  27 421 

Center  Sec.  28 367 

Mid.  E.  hf.Sec.  29 480 

Mid.  W.  hf.  Sec.  29 450 

Center  Sec.  30 420 

Mid.  W.  line  Sec.  30 480 

Mid.  W.  line  Sec.  31 465 

Oak  Hall,  center  Sec.  33 354 

Mid.  E.  line  Sec.  33 353 

Center  Sec.  34 34-5 

Mid.  W.  hf.  Sec.  36 407 

Center  Sec.  36 385 

Dunn.    T.  6,  R.  10  E. 
Road  forks,  E.  line  N.  E.  qr.  Sec.  1.  280 
Road  forks,  W.  line  N.  W.  qr.  Sec.  1  290 

Mid.  N.  hf.  Sec.  2 / 320 

Creek  crossing,   center  N.  W.   qr. 

Sec.  7 255 

Mid.  E.  hf.  Sec.  16 315 

Mid.  W.  hf.  Sec.  16 315 

Mid.  W.  line  Sec.  16 300 

Creek  crossing,  S.  line  S.  W.  qr.  Sec. 

16 270 

Center  Sec.  17 265 

Center  S.  line  Sec.  17 290 

Creek  crossing,  N.  W.  qr.  Sec.  18. .  255 

S.  W.  cor.  Sec.  18 270 

Mid.  E.  line  Sec.  19 330 

Stream  crossing,  near  center  Sec.  20  316 

S.  W.  cor.  Sec.  20 340 

Center  Sec.  21 325 

Center  S.  line  Sec.  21 325 

Center  S.  line  S.  W.  qr.  Sec.  21. ...  360 

S.  E.  cor.  Sec.  21 293 

Mid.  E.  line  S.  E.  qr.  Sec.  21 354 

Mid.  S.  line  Sec.  22 285 

S.  W.  cor.  Sec.  23 298 

Mid.  S.  line  Sec.  25 275 

Mid.  E.  line  Sec.  31  . .   360 

Mid.  S.  line  Sec.  33 315 

Mid.  S.  line  S.  E.  qr.  Sec.  33 275 

Mid.  S.  line  S.  W.  qr.  Sec.  34 275 

Mid.  S.  line  S.  W.  qr.  Sec.  35 295 

Pleasant  Springs.    T.  6.  R.  11  E. 
Bend  in  road,  S.  line  S.  W.  qr.  Sec.  2  350 

Mid.  S.  line  Sec.  3 350 

S.  W.  cor.  Sec.  3 a35 

Mid.  W.  line  Sec.  3 400 

N.  W.  cor.  Sec.  3 400 

Mid.  S.  line  Sec.  4 380 

Mid.  W.  hf.  Sec.  4 325 


Pleasant  Springs.  T.  6.  R.  11  E.— (con.) 

Mid.  S.  line  S.  E.  qr.  Sec.  6 340 

Center  S.  line  Sec.  8 270 

S.  E.  cor.  Sec,  8 285 

S.  E.  cor.  Sec.  9 329 

Mid.  E.  line  Sec.  9 340 

Quarry,  N.  E.  qr.  N.  E.  qr.  See.  10.  410 

Mid.  N.  hf.  Sec.  11 280 

Center  S.  E.  qr.  Sec.  11 320 

Mid.  N.  hf.  Sec.  13. 320 

Mid.  E.  line,  S.  E.  qr.  Sec.  13 325 

S.  E.  cor.  Sec.  13 370 

Mid.  W.  line  N.  W.  qr.  Sec.  13. ..  300 

S.  W.  cor.  Sec.  14 320 

Mid.  S.  line  See.  15 290 

Mid.  W.  line  S.  W.  qr.  Sec.  15  ...  260 

Mid.  S.  line  Sec.  17 265 

Center  Sec.  22 268 

Mid.  S.  line  Sec.  22 340 

S.  E.  cor.  Sec.  24 400 

Mid.  E.  line  Sec.  25 380 

Mid.  W.  line  Sec.  31 305 

Center  Sec.  31 300 

Center  Sec.  32 280 

Mid.  W.  hf.  Sec.  34 308 

Mid.  N.  hf.  Sec.  34 260 

Mid.  W.  hf .  Sec.  35 340 

Mid.  E.  line  Sec.  36 310 

S.  E.  cor.  Sec.  36 350 

Christiana.    T.  6.  R.  12  E. 

Mid.  W.  line  Sec.  2 290 

Mid.  E.  hf .  Sec.  3 280 

N.  W.  cor.  Sec.  6 315 

Mid.  S.  line  S.  E.  qr.  Sec.  6 285 

Stream  crossing,  N.  hf.  Sec.  7 275 

Mid.  S.  hf.  Sec.  7 330 

Mid.  E.  hf .  Sec.  10 320 

Mid.  W.  hf.  Sec.  11 280 

Mid.  E.  line  Sec.  11 260 

Mid.  N.  hf.  Sec.  12 230 

Mid.  E.  hf.  Sec.  12 230 

Stream  crossing,  mid.  W.  line  Sec.  14  290 

S.  E.  cor.  Sec.  15 325 

Mid.  S.  line  Sec.  15 350 

Mid.  E.  line  N.  E.  qr.  Sec.  15 315 

Mid.  S.  line  Sec.  16 385 

S.  W.  cor.  Sec.  16 400 

Mid.  S.  line  S.  E.  qr.  Sec.  17 410 

S.  W.  cor.  Sec.  17 355 

Center  Sec.  18 315 

Mid.  S.  line  Sec.  18 340 

Stream,  E.  line  S.  E.  qr.  Sec.  21.. ..  315 

Mid.  E.  line  S.  E.  qr.  Sec.  22 360 

S.  E.  cor.  Sec,  22 320 

Cross-roads,  S.  line  S.  E.  qr.  Sec.  23.  310 

N.  W.  cor.  Sec.  27 375 

Cross  Plains.    T.  7,  R.  7  E. 

Mid.  E.  line  Sec.  1 400 

Cross  Plains  depot,  Sec.  3. .    274 

Top  of  bluff,  N.  line  N.  W.  qr.  Sec.  3.  420 

Mid.  S.  line  Sec.  3 400 

Mid.  E.  line  N.  E.  qr.  Sec.  7 345 

Center  Sec.  10 325 

Center  S.  E.  qr.  Sec.  10 : . . .  330 

Mid.  E.  line  Sec.  11 326 


SURFACE  RELIEFS. 


BAROMETRICAL  ALTITUDES  —  continued. 


Cross  Plains.    T.  7,  R.  7  E.  —  (con.) 

Mid.  E.  line  S.  E.  qr.  Sec.  12 339 

Mid.  W.  line  N.  W.  cor.  Sec.  15. ..  480 

Center  S.  W.  qr.  Sec.  15 490 

Mid.  S.  line  S.  W.  qr.  Sec.  15 400 

Mid.  N.  hf.  Sec.  17 325 

Mid.  W.  line  N.  W.  qr.  Sec.  17. ...  340 

Mid.  E.  line  Sec.  19 550 

Mid.  E.  line  N.  E.  qr.  Sec.  19 480 

Mid.  E.  line  S.  E.  qr.  Sec.  19 595 

S.  E.  cor.  Sec.  19 570 

Mid.  S.  line  Sec.  20 495 

S.  E.  cor.  Sec.  21 490 

Mid.  W.  hf.  Sec.  22 390 

Mid.  W.  line  S.  W.  qr.  Sec.  27 405 

Stream,  center  S.  E.  qr.  Sec.  33 405 

Middleton.    T.  7,  R.  8  E. 

Road  forks,  E.  hf .  Sec.  2 367 

Mid.  W.  line  Sec.  2 367 

Center  Sec.  3 367 

Center  Sec.  4 447 

Mid.  W.  line  Sec.  4 407 

Mid.  E.  hf.  Sec.  5 421 

Mid.  W.  hf .  Sec.  5  : 507 

Mid.  E.  hf.  Sec.  6 547 

Mid.  W.  hf .  Sec.  6 527 

Mid.  W.  line  S.  W.  qr.  Sec.  7 339 

Center  Sec.  9 352 

Center  Sec.  10 365 

Stream  crossing,  N.  hf.  Sec.  11 357 

Road  forks.  E.  hf .  Sec.  12 320 

Mid.  E.  line  Sec.  13 345 

Mid.  S.  line  Sec.  13 415 

Mid.  S.  line  Sec.  14 410 

S.  W.  cor  Sec.  14 390 

Mid.  S.  line  S.  E.  qr.  Sec.  15 380 

Mid.  W.  line  Sec.  16 553 

Mid.  W.  hf.  Sec.  17 453 

Mid.  S.  hue  Sec.  17 518 

Center  S.  W.  qr.  Sec.  17 555 

Mid.  S.  line  S.  W.  qr.  Sec.  17 518 

Mid.  E.  line  N.  E.  qr.  Sec.  18 353 

Center  N.  E.  qr.  Sec.  18 428 

20  rods  south  of  last 541 

Mid.  N.  hf.  Sec.  20 540 

Mid.  S.  hf.  Sec.  20 503 

b  E.  cor.  Sec.  20 508 

Mid.  S.  line  Sec.  21 538 

Mid.  S.  line  S.  W.  qr.  Sec.  22 508 

Mid.  S.  line  S.  E.  qr.  Sec.  22 478 

S  E.  cor.  sec.  23 450 

Mid.  S.  line  Sec.  24 425 

Mid.  S.  line  Sec.  27 498 

S  W.  cor.  Sec.  27 550 

S.  W.  cor.  Sec.  28 495 

Mid.  S.  line  Sec.  29 480 

S  W.  cor.  Sec.  29 535 

Mid.  E.  line  Sec.  31 540 

Mid.  E.  line  N.  E.  qr.  Sec.  31 600 

S.  W.  cor.  Sec.  32 560 

Center  Sec.  34 508 

Mid.  S.  line  Sec.  34 478 

S.  E.  cor.  Sec.  34 558 

Mid.  S.  Hue  S.  W.  qr.  Sec.  35 513 

Mid.  S.  line  S.  E.  qr.  Sec.  35 433 


Middleton.    T.  7,  R.  8  E.  —  (con.) 

Center  Sec.  35 448 

Mid.  E.  line  S.  E.  qr.  Sec.  35 530 

Mid.  E.  line  Sec.  35 428 

Center  Sec.  36 488 

Mid.  E.  hf.  Sec.  36 458 

Madison.    T.  7,  R.  9  E. 

Lake  Mendota 270 

Capitol  Hill,  S.  W.  cor.  Sec.  13  ....  348 

University  Hill,  S.  W.  cor.  Sec.  14  .  372 

Railroad,  S.  line  Sec.  16 260 

Mid.  S.  line  Sec.  18 332 

Mid.  S.  line  S.  W.  qr.  Sec.  19 450 

Mid.  S.  line  Sec.  19 415 

S.  E.  cor.  Sec.  19 400 

Mid.  S.  line  S.  W.  qr.  Sec.  20 360 

Mid.  S.  line  S.  E.  qr.  Sec.  20 435 

Mid.  S.  line  S.  W.  qr.  Sec.  21 415 

Center  N.  W.  qr.  S.  E.  qr.  Sec.  21  .  390 

Lake  Monona 262 

Road,  mid.  S.  line  Sec.  26 315 

Center  S.  W.  qr.  Sec.  28 295 

S.  line  S.  W.  qr.  S.  W.  qr.  Sec.  28.  360 

Mid.  W.  line  Sec.  31 478 

CenterSec.31 458 

Mid.  E.  line  Sec.  31 448 

Mid.  W.  hf.  of  E.  hf.  of  Sec.  32. ...  438 

Mid.  S.  hf .  Sec.  33 320 

Mid.  E.  line  Sec.  34 290 

Center  Sec.  35 300 

Blooming  Grove.    T.  7,  R.  10  E. 

Mid.  N.  line  N.  W.  qr.  Sec.  3 338 

Mid.  E.  hf .  Sec.  4 315 

Mid.  W.  hf.  Sec.  9 325 

Center  Sec.  9 310 

Mid.  W.  hf.  E.  hf.  Sec.  10 390 

Mid.  W.  hf.  W.  hf.  Sec.  11 410 

Mid.  W.  hf.  Sec.  11 455 

Mid.  W.  hf.  Sec.  12 400 

%  mile  W.  of  center  of  Sec.  12  ....  330 

Center  N.  E.  qr.  Sec.  15 340 

Center  S.  line  S.  E.  qr.  Sec.  15 290 

S.  W.  corner  Sec.  15 310 

Mid.  W.  hf .  Sec.  16 310 

Mid.  W.  hf.  E.  hf.  Sec.  20 320 

Mid.  W.  line  Sec.  21 330 

Center  S.  W.  qr.  Sec.  21 290 

Center  S.  E.  qr.  S.  E.  qr.  Sec.  21 ...  270 

N.  W.  cor.  Sec.  22 310 

Center  S.  E.  qr.  Sec.  22 290 

Mid.  W.  hue  Sec.  26 290 

YK  mile  E.  of  W.  line  Sec.  27  ....  280 

Mid.  N.  line  Sec.  30 300 

Mid.  W.  line  N.  E.  qr.  Sec.  30  ....  310 

One-sixth  mile  E.  N.  W.  cor.  Sec.  35.  350 

Center  Sec.  35 340 

Cottage  Grove.    T.  7,  R.  11  E. 

Mid.  N.  line  Sec  1  320 

Mid.  E.  line  Sec.  1 350 

Center  N.  W.  qr.  Sec.  1 295 

Mid.  W.  line  S.  W.  qr.  Sec.  2 365 

Center  S.  W.  qr.  N.  W.  qr.  Sec.  2  .  275 

Mid.  W.  line  S.  E.  qr.  Sec.  3 360 

Mid.  W.  line  N.  E.  qr.  Sec.  4 320 

Mid.W.  line  S.W.  qr.  S. W.  qr.  Sec.  55  35 


438 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


BAROMETRICAL  ALTITUDES  —  continued. 


Cottage  Grove.    T.  7,  R.  11  E.  — (con.) 

Center  Sec.  6 330 

Mid.  N.  hf.  Sec.  7 325 

Mid.  E.  line  N.  E.  qr.  Sec.  7 345 

Mid.  N.  hf.  Sec.  8 345 

Mid.  E.  line  Sec.  8 315 

Mid.  N.  hf .  Sec.  9  320 

Mid.  S.  hf.  Sec.  9 300 

Center  N.  W.  qr.  Sec.  10 300 

Mid.  N.  hf.  Sec.  10 340 

Mid.  E.  line  N.  E.  qr.  Sec.  10 270 

Mid.  S.  hf.  Sec.  11 300 

Mid.  N.  hf  of  N.  E.  qr.  Sec.  11  ....  345 

Center  of  S.  W.  qr.  Sec.  12 360 

%  mile  S.  mid.  E.  line  N.  E.  qr. 

Sec.  13 275 

Mid.  N.  hf  Sec.  13 275 

TV  mile    S.   W.  of  N.  E.  cor.  of 

Sec.  14 320 

i1*  mile  E.  of  center  of  Sec.  14  .   . . .  330 
1  mile  N.  E.  of  S.  W.  cor.  Sec.  19  . .  280 

Mid.  W.  line  S.  W.  qr.  Sec.  21 280 

Mid.  N.  line  Sec.  21 260 

N.  E.  cor.  Sec.  21 300 

Mid.  S.  line  S.  E.  qr.  Sec.  29 240 

Mid.  S.  line  Sec.  29 300 

Mid.  S.  hf.  S.  W.  qr,  Sec.  29 310 

Mid.  W.  line  Sec.  29 280 

Y»  mile  S.  E.  N.  E.  cor.  Sec.  30. ...  280 

Mid.  E.  hf  Sec.  32   255 

Mid.  N.  hf  Sec.  33 350 

S.  E.  cor.  Sec.  33 420 

Mid.  E.  line  S.  E  qr.  Sec.  33 340 

Deerfleld.    T.  7,  R.  12  E. 

Mid.  N.  line  Sec.  4 320 

Mid.  S.  hf  Sec.  4 290 

Center  S.  E.  qr.  S.  E.  qr.  Sec.  5  ....  335 

Mid.  E.  line  Sec.  7 325 

S.  W.  cor.  S.  E.  qr.  S.  E.  qr.  Sec.  8.  285 

Mid.  N.  hf  Sec.  9 325 

Mid.  W.   line  S.   E.   qr.  S.  E.  qr. 

Sec.  9 280 

Mid.  S.  hf  Sec.  10 265 

Mid.  S.  hf  Sec.  11 275 

Mid.  W.  hf  Sec.  12 290 

Center  S.  W.  qr.  S.  W.  qr.  Sec.  12.  310 

Mid.  S.  hf  Sec.  12..  300 

S.  E.  corner  Sec.  12 270 

Mid.  E.  line  Sec.  13 265 

Mid.  S.  line  Sec.  13 250 

Crossroads.  N.  W.  qr  Sec.  14 285 

Road  corners  E.  line  N.  E.  qr.  Sec. 

18 295 

Center  S.  E.  qr.  Sec.  23 325 

Mid.  W.  hf  Sec.  25 280 

Mid.  W.  line  N.  W.  qr.  Sec.  25. ...  270 

Road  corners,  S.  E.  qr.  Sec.  26 260 

Mid.  E.  hf  Sec.  28 280 

Mid.  S.  line  S.  E.  qr.  Sec.  29 360 

S.  E.  cor.  Sec.  31 320 

Center  S.  E.  qr.  Sec.  32 300 

Center  N.  W.  qr.  Sec.  33 365 

S.  E.  cor.  Sec.  33 305 

S.  E.  cor.  Sec.  34 305 

Mid.  S.  line  S.  E.  qr.  Sec.  35 290 


Deerfleld.    T.  7,  R.  12  E.  —  (con.) 
Mid.  S.  line  Sec.  36 300 

Berry.    T.  8,  R.  7  E. 
Mid.  S.  iine  S.  E.  qr.  Sec.  3  ........  340 

S.  W.  cor.  Sec.  3 330 

Mid.  W.  line  Sec.  3 340 

Mid.  S.  line  Sec.  5 330 

Center  Sec.  7 280 

Roadforks,  N.  W.  qr.  Sec.  8 280 

Roadforks,  N.  W.  qr.  Sec.  9 310 

Mid.  S.  line  Sec.  9  450 

Mid.  S.  line  S.  E.  qr.  Sec.  10 4oO 

Center  S.  E.  qr.  Sec.  10 365 

Mid.  S.  line  S.  W.  qr.  Sec.  13 440 

Mid.  E.  line  S.  W.  qr.  Sec.  13 515 

S.  W.  cor.  Sec.  14 540 

Road  forks,  N.  PI  qr.  Sec.  15 385 

S.  W.  cor.  Sec.  15 370 

Center  N.  W.  qr.  Sec.  15 380 

Center  S.  E.  qr.  Sec.  16 350 

Center  Sec.  16 435 

Mid.  N.  hf .  Sec.  16 475 

Mid,  S.  line  S.  W.  qr.  Sec.  16 300 

Center  N.  E.  qr.  Sec.  17 500 

Mid.  N.  hf .  Sec.  17 465 

Mid.  N.  hf.  Sec.  18 445 

Mid.  W.  line  Sec.  18 440 

N.  W.  cor.  Sec.  21 275 

Mid.  W.  line  Sec.  21 310 

Mid.  E.  hue  N.  E.  qr.  Sec.  21 450 

Mid.  E.  line  Sec.  21 540 

Mid.  S.  line  S.  W.  qr.  Sec.  22 350 

Mid.  E.  line  Sec.  22 400 

Mid.  N.  hf .  Sec.  23 450 

Road  corners,  N.  E.  qr.  Sec.  23 510 

Mid.  E.  line  S.  E.  qr.  Sec.  24 415 

S.  E.  corner  Sec.  24 360 

Mid.  E.  hf.  Sec.  25 340 

Mid.  W.  line  Sec.  25 400 

Center  Sec.  27 335 

Mid.  S.  hf.  Sec.  27 345 

Road-forks  S.  E.  qr.  Sec.  27 440 

Road  corners  S.  W.  qr.  Sec.  27 330 

Center  S.  E.  qr.  Sec.  29 '. .  480 

Center  N.  E.  qr.  Sec.  29 490 

Mid.  E.  hf.  Sec.  29 460 

Center  N.  E.  qr.  Sec.  32 430 

Mid.  S.  line  S.  E.  qr.  Sec.  33 310 

Mid.  E.  line  Sec.  33 290 

Mid.  E.  line  N.  E.  qr.  Sec.  34 520 

Mid.  S.  line  Sec.  35 320 

Center  N.  E.  qr.  Sec.  35 400 

Mid.  E.  hf.  Sec.  35 325 

Center  N.  E.  qr.  Sec.  36 460 

Springfield.    T.  8,  R.  8  E. 

Mid.  S.  line  S.  W.  qr.  Sec.  1 420 

Mid.  S.  line  S.  W.  qr.  Sec.  2 335 

Mid.  S.  line  Sec.  3 350 

Mid.  S.  hf.  of  N.  hf.  Sec.  4 410 

Center  Sec.  4 480 

Road-forks  W.  line  Sec.  5 410 

Road-forks  S.  W.  qr.  Sec.  8 520 

Mid.  E.  hf .  N.  W.  qr.  Sec.  8 480 

Road  corners  N.  E.  qr.  Sec.  9. . : . . .  350 
Mid.  W.  line  S.  W.  qr.  Sec.  10  ....  340 


SURFACE  BELIEFS. 


439 


BAROMETRICAL  ALTITUDES  —  continued. 


Springfield.    T.  8,  R.  8  E.  — (con.) 

Center  N.  W.  qr.  Sec.  12 

Mid.  W.  hf.  Sec.  15 

Mid.  S.  line  Sec.  15 

S.  W.  cor.  Sec.  15 

Mid.  S.  line  S.  W.  qr.  Sec.  16 

Mid.  E.  hf .  Sec.  17 

Mid.  W.  line  Sec.  17 

Mid.  W.  line  N.  W.  qr.  Sec.  17. . . . 

S.part  N.E.qr.Sec.18 

S.part  S.E.qr.Sec-18 

Road  corners  S.W.qr.Sec.19 

Center  Sec. 19 

Mid.N.  line  S. W.  qr.S-W.qr.Sec. 
19 

Center  Sec.  21 

Mid.W.hf.Sec-21 

Center  N.  W.  qr.  Sec.  21 

Mid.  W.  hf.  E.  hf.  Sec  22 

Center  Sec.  22 

S.  E.  corner  Sec.  22 

Mid  W.  hf .  Sec.  23   

Mid  S.  line,  Sec.  24   

Mid.  W.  line,  Sec.  25 

Mid.  E.  hf.  E.  hf.  Sec.  26 

Mid  W.  line  Sec.  26 

Center  Sec.  27 

Mid  W.  line,  Sec.  27 

S.  W.  cor.  Sec.  27 

S.  line  S.  W.  qr.  S.  W.  qr.  Sec.  28. 

Center  N.  W.  qr.  Sec.  31 

Mid.  W.  hf .  E.  hf .  Sec.  31 

Center  S.  W.  qr.  N.  E.  qr.  Sec.  31  . 

Center  S.  W.  qr.  Sec.  31  ....   : . . . . 

Mid.  E.  line,  Sec.  33 

Mid.  S.  E.  qr.  Sec.  34 

Westport.  T.  8,  R.  9,  E. 

Mid.  E.  hf.  S.  E.  qr.  Sec.  1      

Center  S.  E.  qr.  Sec.  2 

Waunakee  depot 

Mid  S.  line  S.  E.  qr.  Sec.  6 

S.  E.  cor.  Sec.  7 

Mid.  S.  line  Sec.  11  

S.  E.cor.  Sec,  11 

Mid.  N.  hf .  Sec.  12 

S.  W.  Sec.  17 

Stream  crossing,  E.  hf.  Sec.  19 

Bluff-top  N.  hf.  Sec.  19 

Mid.  S.  line  S.  E.  qr.  Sec.  19 

Mid.  E.  line  Sec.  19   

Roadforks,  N.  E.  qr.  Sec.  22    

Mid.  N.  hf.  Sec.  23 

Quarry,  N.  line  S.  W.  qr.  Sec.  25. .. 

Mid.  S.  line  Sec.  25   

Center  Sec.  26 

Mid.  E.  line  S.  E.  qr.  Sec.  36 

Burke.  T.  8,  R.  10  E. 

Mid.  E.  line  Sec.  1 

Mid.  N.  Line.  Sec.  3 

Quany,  S.  W.  qr.  S.  W.  qr.  Sec.  2  . 

Creek,  N.  line  N.  W.  qr.  Sec.  3 

N.  W.  cor.  Sec.  4 

N.  W.cor.Sec.5 

N.  W.  cor.  Sec.  6 

Mid.  S.  line  Sec.  8 


aso 

395 
400 
450 
520 
520 
450 
450 
402 
380 
375 
380 

450 
480 
450 
480 
370 
429 
390 
450 
350 
390 
430 
390 
380 
420 
380 
450 
525 
500 
560 
450 
350 
360 

300 
350 
341 
335 
390 
403 
403 
320 
325 
290 
400 
295 
325 
277 
371 
394 
290 
340 
310 

400 
296 
460 
285 
307 
295 
282 
302 


Burke.    T.  8,  R.  10E.  —  (con.) 

1-8  mile  E 392 

S.  E.  comer  Sec.  8 332 

Mid.  S.  line  Sec.  9 334 

S.  E.  cor.  Sec.  9   354 

Mid.  S.  line  Sec.  10  380 

S.  E.  cor.  Sec.  10   380 

School,  N.  W.  cor.  Sec.  13 332 

Center  Sec.  12 327 

Mid.  S.  hf.  Sec.  14 372 

S.  W.  cor.  Sec.  17 277 

Mid.  N.  hf .  Sec.  19 292 

Mid.  S.  line  Sec.  19 327 

Mid.  E.  line  Sec.  21  314 

Mid.  E.  line  S.  E.  qr.  Sec.  21 354 

Center  Sec.  22 390 

Mid.  S.  line  Sec.  22   340 

Railroad,  E.  line  N.  E.  qr.  Sec.  23. .  355 

Quarry.  N.  W.  qr.  Sec.  27 325 

Mid.  W.  line  Sec.  28 308 

Center  Sec.  29 280 

Center  Sec.  30 302 

Mid.  S.  line  Sec.  30 302 

Center  Sec.  31 392 

Crossroads  N.  W  qr.  Sec.  33 315 

Mid.  E.  line  N.  E.  qr.  Sac.  33 274 

Mid.  W.  hf .  Sec.  35 420 

Quarry,  N.  E.  qr.  N.  W.  qr.  Sec.  35  462 

Sun  Prairie.    T.  8,  R.  11  E. 

Mid.  W.  line  S.  W.  qr.  Sec.  1 315 

S.  E.  cor.  Sec.  13 330 

Mid.  S.  line  S.  E.  qr.  Sec.  13 350 

Center  Sec.  24 350 

Medina.    T.  8,  R.  12  E. 

Mid.  W.  line  Sec.  1 290 

S.  W.  cor.  Sec.  1 250 

Mid.  S.  line  S.  W.  qr.  Sec.  2 260 

Mid.  S.  line  Sec.  3 315 

S.  W.  cor  Sec.  3 315 

Mid.  N.  line  Sec.  4 300 

Stream,  W.  line  Sec.  4 280 

Mid.  E.  line  Sec.  7 320 

S.  E.cor.  Sec.  7 320 

Mid.  E.  line  Sec.  11 255 

N.  W.  cor.  Sec.  13 295 

Mid.  W.  line  Sec.  13 255 

S.  W.  cor.  Sec.  13 270 

Mid.  S.  line  Sec.  14 305 

Mid.  E.  hf.  Sec.  15 ...     260 

Marshall,  Sec.  15 290 

Center  S.  W.  qr.  Sec.  16 280 

Mid.  W.  line  N.  W.  qr.  Sec.  16. ...  295 

Center  Sec.  17 300 

S.  W.cor.Sec,  18 330 

S.  E.  cor.  Sec.  20 305 

Mid.  E.  line  Sec.  22 315 

S.  E.  cor.  Sec.  22 360 

Mid.  S.  hf.  Sec.  23 370 

Mid.  S.  line  Sec.  23 360 

Mid.  N.  hf.  Sec.  24 320 

Mid.  S.  line  S.  E.  qr.  Sec.  24 300 

Mid.  S.  line 'Sec.  25 365 

S.  W.  cor.  Sec.  25 315 

Mid.  N.  hf.  Sec.  26 420 

Mid.  S.  line  Sec.  26 390 


440 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


BAROMETRICAL  ALTITUDES  —  continued. 


Medina.    T.  8,  R.  12  E.  —  (con.) 

Mid.  E.  line  N.  E.  qr.  Sec.  27 320 

Stream,  N.  W.  qr.  Sec.  27 290 

Mid.  E.  hf,  Sec.  29 310 

Mid.  S.  line  Sec.  29 315 

Center  Sec.  32 290 

Mid.  S.  line  Sec.  32 320 

Center  Sec.  33. 338 

Mid.  \V.  M .  Sec.  33 300 

Mid.  N.  hf.  Sec.  33 340 

Mid.  S.  M.  Sec.  33 340 

Center  N.  W.  qr.  Sec.  36 305 

Roxbury.    T.  9,  R.  7  E. 

S.  W.  cor.  Sec.  3 275 

S.  W.  cor.  Sec.  4 265 

Bluff  near  center  Sec.  5 430 

Center  S.  E.  qr.  Sec.  5 250 

Road  crossing,  mid.  S.  hf.  W.  line 

Sec.  5 285 

Center  N.  E.  qr.  S.  E.  qr.  Sec.  6. ...  310 

Mid.  E.  line  Sec.  7 275 

Mid.  S.  line  Sec.  7 200 

Mid.  S.  line  S.  E.  qr.  Sec.  7 200 

Mid.  S.  line  S.  E.  qr.  N.  E  qr.  Sec.7  300 

Center  S.  E.  qr.  N.  W.  qr.  Sec.  8. . .  450 

S.  E.  cor.  Sec.  8 320 

N.  E.  qr.  S.  E.  qr.  Sec.  9 350 

S.  W.  cor.  Sec.  10 340 

Forks  of  road,  S.  E.  qr.  Sec.  10 330 

Mid.  E.  line  S.  E.  qr.  Sec.  10 305 

S.  line  S.  E.  qr.  S.  W.  qr.  Sec.  10  ..  340 

S.  line  S.  W.  qr.  S.  E.  qr.  Sec.  10  . .  285 

Mid.  E.  line  N.  E.  qr.  Sec.  11 400 

Mid.  N.  hf.  Sec.  11 340 

N.  W.  cor.  Sec.  12 430 

Mid.  N.  hf.  Sec.  12 340 

Center  N.  E.  qr.  S.  W.  qr.  Sec.  12. .  500 

Center  N.  W.  qr.  S.  E.  qr.  Sec.  12. .  410 

Mid.  E.  line  Sec.  12 430 

S.  W.  cor.  Sec.  12 365 

S.  E.  cor.  Sec.  12 370 

Mid.  N.  line  N.  W.  qr.  Sec.  13 430 

Mid.  S.  hf.  Sec.  13 370 

Mid.  W.  hf.  Sec.  13 330 

Mid.  S.  line  Sec.  13 400 

Center  N.  E.  qr.  Sec.  14 271 

Mid.  S.  line  Sec.  16 270 

Mid.  S.  line  S.  W.  qr.  Sec.  16 270 

Mid.  S.  line  S.  E.  qr.  Sec.  17 255 

S.  W.  cor.  Sec.  17 255 

Mid.  E.  line  N.  E.  qr.  Sec.  19 215 

Mid.  N.  hf.  S.  hf.  Sec.  20 205 

Mid.  S.  line  S.  W.  qr.  Sec.  21 375 

Mid.  E.  line  Sec.  22 305 

Mid.  N.  W.  qr.  Sec.  23 305 

Mid.  E.  line  N.  E.  qr.  Sec.  23 410 

Mid.  N.  line  N.  W.  qr.  See.  24 425 

Mid.  E.  line  Sec,  24 530 

Mid.  E.  line  Sec.  25 500 

S.  E.  cor.  Sec.  25 550 

S.  W.  cor.  Sec.  25 390 

Aldens  Corner,  Sec.  26 365 

Mid.  W.  line  S.  W.  qr.  Sec.  27 305 

Mid.  W.  line,  Sec.  28 290 

Mid.  W.  line  N.  W.  qr.  Sec.  28. ...  280 


Roxbury.    T.  9,  R.  7  E.  —  (con.) 
Mid.  W.  line  N.  W.  qr.  Sec.  29  .... 

Center  S.  E.  qr.  Sec.  30  ......  :  ____ 

Center  N.  E.  qr.  N.  E.  qr.  Sec.31  ... 
Center  S.  E.  qr.  Sec.  31  .......... 

Center  E.  line  S.  E.  qr.  Sec.  31  ..... 

Center  S.  hf.  Sec.  32  .............. 


Mid.  E.  line  S.  E.  qr.  Sec.  32  ...... 

Mid.  W.  hf.  Sec.  33  ............... 

Mid.  E.  hf.  Sec.  33.  .  .............. 

Mid.  E.  line  Sec.  33  ............... 

Center  S.  E.  qr.  Sec.  34  ........... 

Mid.  E.  line  Sec.  36  ............... 

Dane.    T.  9,  R.  8  E. 
Mid.  S.  line  S.  W.  qr.  Sec.  2  ....... 

Mid.  W.  line,  Sec.  2  .............. 

N.  W.  cor.  Sec.  2  ................. 

Center  N.  hf  Sec.  4  .  .   ........... 

%  mile  W  ..................... 

Mid.  W.  line  N.  W.  qr  Sec.  4  ..... 

Mid.  E.  line  Sec.  7  ............... 

S.  E.  cor.  Sec.  7  ................. 

Cross  roads,  N.W.  qr.  S.  E.  qr.  Sec.  7, 
Center  S.  W.  qr.  Sec.  7 


Mid.  S.  line  Sec.  7  ........ 

Center  Sec.  9  ..................... 

Center  Sec.  11  ................... 

S.  E.  cor.  Sec.  11  ................. 

Center  N.  E.  qr.  Sec.  12  ........... 

Mid.  E.  line  Sec.  12  ............... 

Dane  Station,  Sec.  13  ............. 

Mid.  W.  line  Sec.  15  .............. 

S.  W.  cor.  Sec.  15  ................ 

Center  S.  W.  qr.  Sec.  17  ........... 

Mid.  S.  line  S.  W.  qr.  Sec.  17  ...... 

Center  Sec.  19  .................... 

Center  Sec.  20  .................... 

Mid.  S.  line  Sec.  20  .............. 

S.  E.  cor.  Sec.  20  ................. 

Mid.  S.  line  S.  W.  qr.  Sec.  23  ...... 

Mid.  S.  line  S.  E.  qr.Sec.  23  ........ 

Mid.  W.  line  Sec.  27  .............. 

Center  N.  W.  qr.  Sec.  30  .......... 

Mid.  W.  line  S.  W.  qr.  Sec.  31  .... 

Center  S.  E.  qr.  Sec.  33  ......... 

Vienna.  T.  9,  R.  9  E.  — 

Mid.  W.  hf.  Sec.  7  ............... 

Mid.  W.  line  Sec.  7  .............. 

Mid.  E.  hf  .  Sec.  7  ................. 

Mid.  W.  hf.  Sec.  8  ................ 

Center  Sec.  8  ..................... 

Mid.  S.hf.  Sec.  8  ................. 

S.  W.  cor.  Sec.  15  ................. 

Knob,  S.  hf.  Sec.  20  ............... 

Mid.  E.  line  Sec.  21  ............. 

Mid.  W.  line  Sec.  27  ............. 

Windsor.  T.  9,  R.  10  E. 

Mid.  S.  line  S.  W.  qr.  Sec.  1  ....... 

Mid.  S.  line  S.  E.  qr.  Sec.  2  ........ 

Mid.  S.  line  Sec.  2  ............... 

S.  W.  cor.  Sec.  2  .................. 

Mid.  S.  line,  S.  W.  qr.  Sec.  3  ....... 

Mid.  S.  line  S.  E.  qr.  Sec.  4.  ...:... 


315 

490 
390 
255 
265 
285 
340 
375 
385 
505 
400 
380 
600 

320 
375 
300 
280 
500 
520 
355 
410 
330 
425 
500? 
540 
380 
420 
510 
400 
500 
477 
440 
550 
510 
445 
490 
450 
500 
560 
445 
560 
560 
590 
560 
480 

540 
500 
530 
470 
500 
440 
480 
520 
490 
540 

416 
426 
426 
416 
396 
436 


SURFACE  RELIEFS. 


441 


BAROMETRICAL  ALTITUDES  —  continued. 


Windsor.    T.  9,  R.  10  E.  —  (con.) 

Mid.  S.  line  Sec.  4 416 

Center  N.  W.  qr.  Sec.  10 406 

Center  N.  W.  qr.  S.  E.  qr.  Sec.  10. .  396 

S.  W.  corner  Sec.  10 376 

Mid.  E.  hf.  Sec.  11 411 

Mid.  S.  line  Sec,  11 416 

S.  E.  cor.  Sec.  11 416 

Center  N.  W.  qr.  Sec.  13 396 

Mid.  W.  line  S.  W.  qr.  Sec.  13 416 

Quarry,  S.  E.  qr.  Sec.  14 466 

Forks  of  road,  S.  E.  cor.  Sec.  14. ...  426 

N.  W.  qr.  Sec.  16 376 

Mid.  W.  line  N.  W.  qr.  Sec.  16. ...  386 

S.  W.  cor.  Sec.  16 386 

Mid.  W.  line  N.  W.  qr.  Sec.  21. ...  401 

Mid.  W.  line  S.  W.  qr.  Sec.  21 405 

Mid.  E.  line  Sec.  23 416 

S.  E.  cor.  Sec.  23 376 

Mid.  W.  line  Sec.  25 396 

S.  W.  cor.  Sec.  25 386 

Mid.  S.  line  S.  E.  qr.  Sec.  25 346 

Mid.  N.  line  Sec.  25 356 

S.  E.  cor.  Sec.  25 356 

Mid.  S.  line  Sec.  26 306 

Mid.  S.  line  S.  E.  qr.  Sec.  27 336 

Mid.  W.  hf.  Sec.  27 386 

Center  N.  W.  qr.  Sec.  28 396 

Mid.  E.  hf.  Sec.  28 411 

Mid.  W.  line  Sec.  28 366 

Center  Sec.  29 326 

Forks  of  road,  N.  W.  qr.  Sec.  34... .  311 
Center  N.  W.  qr.  Sec.  35 336 

Bristol.    T.  9,  R.  11  E. 

Mid.  S.  line  S.  W.  qr.  Sec.  1 366 

S.  W.  cor.  Sec.  1 346 

Mid.  S.  line  S.  E.  qr.  Sec.  2 376 

Mid.  S.  line  Sec.  3 376 

Mid.  W.  line  Sec.  3 356 

Mid.  S.  line  Sec.  4 376 

Mid.  E.  hf.  Sec.  5 371 

Mid.  S.  line  Sec.  5 366 

Mid.  S.  line  S.  W.  qr.  Sec.  5 366 

Mid.  S.  line  S.  E.  qr.  Sec.  6 386 

Mid.  E.  hf.  Sec.  7 366 

Mid.  S.  line  S.  E.  qr.  Sec.  7 356 

N.  W.  cor.  Sec.  9 366 

Center  S.  E.  qr.  Sec.  9 376 

Center  N.  E.  qr.  Sec.  9 36G 

Mid.  S.  line  S.  W.  qr.  S.  W.  qr. 

Sec.  10 376 

Mid.  E.  line  Sec.  10 376 

Mid.  E.  line  N.  E.  qr.  Sec.  11 376 

S.  E.  cor.  Sec.  12 366 

Center  Sec.  13 371 

Mid.  E.  hf.  Sec.  16 371 

Mid.  E.  hf .  Sec.  17 416 

Mid.  S.  line  Sec.  17  406 

Mid.  S.  line  S.  E.  qr.  Sec.  18 386 

N.  W.  cor.  Sec.  20 396 

Center  N.  E.  qr.  Sec.  20 381 

S.  W.  cor.  Sec.  20 406 

%  mile  south 406 

Mid.  E.  line  S.  E.  qr.  Sec.  21 366 

S.  E.  cor.  Sec.  21 356 


Bristol.    T.  9,  R.  11  E.—  (con.) 

Mid.  S.  hf.  Sec.  22 386 

Mid.  E.  line  N.  E.  qr.  Sec.  23 371 

Mid.  E.  line  Sec.  23  356 

Center  Sec.  25 336 

S.  W.  cor.  Sec.  25 366 

Center  Sec.  26 376 

Mid.  W.  hf .  Sec.  26 386 

Mid.  W.  line  Sec  26  376 

N.  W.  cor.  Sec.  27 356 

S.  W.  cor.  Sec.  27 416 

Mid.  E.  hf .  Sec.  29 416 

Mid.  S.  line  S.  W.  qr.  Sec.  29 406 

S.  W.  cor.  Sec.  29 376 

S.  W.  cor.  Sec.  30 356 

Mid.  E.  line  N.  E.  qr.  Sec.  31 386 

S.  E.  cor.  Sec.  31 421 

Mid.  E.  hf .  Sec.  32 396 

S.  E.  cor.  Sec.  34 371 

Mid.  E.  line  Sec.  34 376 

N.  W.  cor.  Sec.  35 396 

Mid.  E.  line  Sec.  35 376 

York.    T.  9,  R.  12  E. 

Mid.  W.  hne  S.  W.  qr.  Sec.  1 310 

Mid.  S.  line  S.  W.  qr.  Sec.  1 340 

S.  W.  cor.  Sec.  1 325 

Mid.  N.  line  Sec.  2 335 

S.  W.  cor.  Sec.  2 360 

Mid.  S.  line  Sec.  3 345 

S.  W  cor.  Sec.  3 365 

Mid.  S.  line  Sec.  4 355 

S.  W.  cor.  Sec.  4 3-58 

Mid.  W.  line  S.  W.  qr.  Sec.  4 365 

Center  Sec.  5 355 

Mid.  S.  line  Sec.  6 385 

Center  Sec.  7. 365 

S.  W.  cor.  Sec.  7 345 

Mid.  N.  line  N.  E.  qr.  Sec.  8 36Q 

Mid.  E.  hne  Sec.  8 350 

Mid.  S.  line  S.  E.  qr.  Sec.  8 340 

S.  E.  cor.  Sec.  9 390 

Mid.  S.  line  Sec.  9 360 

Mid.  N.  hf  Sec.  10 345 

Mid.  S.  line  Sec.  10 380 

Mid.  N.  line  Sec.  11  ., 335 

Mid.  E.  hne  Sec.  11 340 

Mid.  S.  line  S.  E.  qr.  Sec.  12 265 

S.  E.  cor.  Sec.  12 290 

S.  E.  cor.  Sec.  13 340 

S.  W.  cor.  Sec.  15 360 

Mid.  W.  line  Sec.  16 350 

Center  Sec.  17 350 

N.  E.  cor.  Sec.  19 320 

Center  Sec.  19 320 

S.  E.  cor.  Sec.  20 330 

Mid.  E.  line  N.  E.  qr.  Sec.  21 340 

S.  E.  cor.  Sec.  21 360 

Mid.  S.  hne  Sec.  21 370 

Center  Sec.  22 375 

Mid.  S.  hne  Sec.  22 350 

Mid.  S.  line  S.  E.  qr.  Sec.  23 375 

S.  E.  cor.  Sec.  24 320 

S.  E.  cor.  Sec.  25 325 

Mid.  S.  line  Sec.  25 335 

Mid.  N.  line  Sec.  26 340 


442 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


BAROMETRICAL  ALTITUDES  —  continued. 


York.    T.  9,  R.  12  E.  —  (con.) 

S.  W.  cor.  Sec.  26 355 

Mid.  S.  line  Sec.  26 375 

Mid.  W.  line  Sec.  27 390 

Mid.  E.  line  Sec.  34 :'..V> 

S.  E.  cor.  Sec.  34 325 

Mid.  E.  line  Sec.  36 330 

West  Point.    T.  10,  R.  7  E. 
Gibraltar  Bluff,  Mid.  E.  line  Sec.  13  6*5 
Marsh  at  foot  of  same,  E.  hf .  Sec.  13  230 
Cemetery,  S.  E.  qr.  S.  E.  qr.  Sec.  14  370 

Mid.  S.  line  S.  E.  qr.  Sec.  15 270 

S.  W.  cor.  Sec.  14 290 

Mid.  S.  line  Sec.  15 280 

S.  line  S.  E.  qr.  Sec.  16 290 

Mid.  S.  line  Sec.  16 280 

Bend  in  road,  N.  line  N.  E.  qr.  Sec. 

20 250 

Top  of  limestone  bluff,  N.  E.  qr. 

Sec.  20 485 

S.  E.  cor.  Sec.  21 320 

Mid.  S.  line  S.  E.  qr.  sec.  22 280 

Mid.  E.  line  Sec.  22 325 

Mid.  S.  line  Sec.  24 420 

Center  S.  E.  qr.  Sec.  25 400 

Mid.  E.hf.  Sec.  27 270 

Center  S.  E.  qr.  Sec.  27 310 

S.  E.  cor.  Sec.  27 275 

Center  S.  W.  qr.  Sec.  27 310 

Mid.  S.  line  S.  W.  qr.   S.  W.  qr. 

Sec.  27 340 

Mid.  E.  line  Sec.  28 330 

S.  W.  cor.  Sec.  28 290 

Mid.  S.  line  S.  W.  qr.  Sec.  29 280 

Road,  S.  E.  qr.  Sec.  31 290 

Mid.  W.  hf.  N.  E.  qr.  Sec.  33 370 

Crossroads,  N.  hf.  Sec.  36 345 

Lodi  (and  West  Point  in  part).  T.  10, 
R.  8E. 

Bluff-top,  S.  W.  qr.  Sec.  7 520 

Road-corners,  N.  W.  qr.  Sec.  14  ...  330 

Mid.  S.  line  S.  W.  qr.  Sec.  14 420 

Mid.  N.  hf .  Sec.  14 475 

Center  N.  W.  qr.  Sec.  15 340 

Center  N.  W.  qr.  Sec.  16 315 

Mid.  E.  line  Sec.  19 310 

Mid.  W.  hf .  Sec.  20 '.  250 

%  mile  S.  of  Cent,  of  Sec.  20 240 

S.  W.  cor.  Sec.  20 440 

Center  N.  W.  qr.  Sec.  23 360 

Mid.  E.  line  N.  E.  qr.  Sec.  23 460 

Mid.  S.  line  S.  W.  qr.  Sec.  23 340 

Bluff-top,  S.  E.  qr.  Sec.  23 560 

Bluff- top,  N.  W.  qr.  Sec.  24 560 

Center  Sec.  26 250 

Center  S.  E.  qr.  Sec.  27 330 

Center  S.  W.  qr.  Sec,  28 470 

Mid.  W.  line  S.  W.  qr.  Sec.  28  ....  420 

Mid.  W.  line  Sec.  29 360 

Bluff-top,  mid.  N.  hf.  Sec.  31 475 

Mid.  E.  line  Sec.  31 350 

Mid.  E.  line  Sec.  32 380 

Arlington.    T.  10,  R.  8  E. 

Creek  crossing,  N.  E.  qr.  Sec.  1 300 

Bluff-top,  S.  E.  cor.  Sec.  2 445 


Arlington.    T.  10,  T.  8  E.  —  (con.) 

S.  W.  cor.  Sec.  2 

Center  Sec.  3 

Creek  crossing,  S.  E.  qr.  Sec.  3 

Mid.  S.  line  S.  W.  qr.  Sec.  4 

S.  W.  cor.  Sec.  4 

S.  W.  cor.  Sec.  5 

Mid.  W.  line  Sec.  5 

S.  line  S.  W.  qr.  Sec.  7 

S.  E.  cor.  Sec.  7 

S.  E.  cor.  Sec.  8 

Mid.  E.  line  Sec.  8 

Mid.  E.  line  Sec.  10 

S.  E.  cor.  Sec.  10 

Mid.  N.  line  N.  W.  qr.  Sec.  13  .... 

Mid.  S.  line  S.  E.  qr.  Sec.  13 

Arlington  station,  Sec.  13 

S.  W.  cor.  Sec.  14 

S.  W.  cor.  Sec.  15 

Mid.  S.  line  Sec.  16 

S.  W.  cor.  Sec.  16 

S.  W.  cor.  Sec.  17 

Mid.  W.  line  Sec.  17 

Center  Sec,  19 

S.  E.  cor.  Sec.  19 

Knob,  S.  line  S.  E.  qr.  Sec.  21 

Mid.  E.  line  S.  E.  qr.  Sec.  21 

Bluff-top,  S.  W.  qr.  Sec.  27 

Bluff-top,  N.  W.  qr.  Sec.  28 

Bluff-top,  W.  line  S.  W.  qr.  Sec.  28. 

Mid.  W.  line  Sec.  28 

S.  W.  cor.  Sec.  29 

Bluff-top,  N.  E.  qr.  Sec.  34 

Columbus.    T.  10,  R.  12  E. 

Mid.  S.  line  Sec.  7 

Stream,  S.  line  S.  E.  qr.  Sec.  8 

Mid.  N.  line  Sec.  9 

N.  E.  cor.  Sec.  9 

N.  E.  cor.  Sec.  16 

N.  W.  cor.  Sec.  17 

Mid.  N.  line  Sec.  17 

W.  line  N.  W.  qr.  Sec.  19 

Mid.  E.  line  Sec.  20 

N.  E.  cor.  Sec.  20 

Mid.  E.  hf.  Sec.  21 

Stream  crossing,  N.  W.  qr.  Sec.  28. 

Mid.  N.  hf.  Sec.  32 

Mid.  E.hf.  Sec.  33 

Dekorra.    T.  11  N.,  R.  8  E. 

Mid.  E.  hf .  Sec.  23 

Mid.  E.  line  Sec.  23 


380 
305 
270 
375 
355 
370 
340 
525 
425 
465 
440 
520 
480 
440 
460 
460 
470 
500 
460 
440 
490 
460 
540 
460 
525 
500 
520 
525 
520 
420 
480 
520 

300 
275 
310 
385 
285 
295 
285 
365 
325 
305 
285 
300 
395 
395 


Dekorra.    T.  11,  R.  9  E. 

Mid.  W.  line  S.  W.  qr.  Sec.  11  . . . 

Cross-roads,  W.  hf.  Sec.  14 

Mid.  W.  line  Sec.  17 

S.  W.  cor.  Sec.  17 

S.  W.  cor.  Sec.  20 

Mid.  S.  line  S.  E.  qr.  Sec.  16 

Cemetery,  W.  hf.  Sec.  23 

Mid.  W.  hf.  Sec.  28 

Stream  crossing,  N.  E.  qr.  Sec.  30. 

Mid.  E.  line  N.  E.  qr.  Sec.  30 

Mid.  S.  hf.  Sec.  33 

Poynette  depot 


280 
335 
340 
370 
220 
380 
310 
320 
220 
240 
270 
264 


SURFACE  RELIEFS. 


443 


BAROMETRICAL  ALTITUDES  —  continued. 


Lowville.    T.  11  K,  R,  10  E. 

S.  E.  cor.  Sec.  1 360 

Mid.  S.  line  S.  W.  qr.  Sec.  2 330 

Mid.  5.  line  S.  W.  qr.  Sec.  3 :!-3> 

Bluff  ^th  mile  north 42-. 

Ravine,  S.  W.  cor.  Sec.  4 260 

S.  W.  cor.  Sec.  5 320 

Mid.  S.  line  S.  W.  qr.  Sec.  6 300 

Mid.  E.  hf .  Sec.  8 280 

Bluff-top,  S.  E.  qr.  Sec.  9 400 

Mid.  S.  line  S.  W.  qr.  Sec.  9 330 

Mid.  S.  line  Sec.  10 350 

S.  W.  cor.  Sec.  11 350 

S.  E.  cor.  Sec.  11 370 

S.  E.  cor.  Sec.  12 370 

Mid.  W.  line  Sec.  13 350 

Mid.  S.  W.  qr.  Sec.  17 310 

Mid.  W.  hf.  Sec.  18 290 

Mid.  E.  line  Sec.  19 340 

Mid.  E.  hf.  Sec.  20 360 

Mid.  S.  line  S.  E.  qr.  Sec.  20 420 

Knob,  S.  line  S.  E.  qr.  Sec.  23 460 

S.  E.  cor.  Sec.  23 400 

Mid.  S.  line  Sec.  24 400 

Mid.  W.  line  N.  W.  qr.  Sec.  28. ...  400 

Cent,  N.  E.  qr.  Sec.  29 420 

Bluff  top.  S.  E.  qr.  Sec.  31 410 

Mid.  E.  line  Sec.  31 350 

Mid.  E.  hf .  Sec.  32 400 

Otseffo.    T.  11,  R.  11  E. 

Mid.  W.  hf.  Sec.  1 345 

Mid.  W.  line  Sec.  1 375 

Cent.  Sec.  2 345 

Mid.  E.  hf.  Sec.  3 330 

Mid.  W.  line  Sec.  3 350 

Cent.  Sec.  4 • 375 

Cent.  Sec.  5 340 

Mid.  W.  line  Sec.  5 360 

Mid.  W.  line  Sec.  7 420 

Mid.  E.  line  Sec.  11 365 

Doylestown,  Sec.  12 360 

S.  W.  cor.  Sec.  15 380 

S.  W.  cor.  Sec.  16 390 

Mid.  S.  line  Sec.  17 365 

S.  W.  cor.  Sec.  17 380 

Mid.  S.  line  Sec.  19 340 

S.  E.  cor.  Sec.  19 350 

Mid.  S.  line  Sec.  20 355 

Cent,  S.  W.  qr.  Sec.  22 360 

Mid.  N.  hf.  Sec.  22 365 

Otsego,  Sec.  22 355 

Stream,  E.  line  N.  E.  qr.  Sec.  23. ..  345 

Mid.  E.  line  Sec.  23 365 

Mid.  E.  line  S.  E.  qr.  Sec.  23 345 

Mid.  E.  hf .  Sec.  32 365 

Mid.  E.  line  Sec.  32 365 

Cent.  Sec.  33 365 

Cent.  Sec.  34 365 

Mid.  W.  hf.  Sec.  35 355 

Mid.  E.  line  Sec.  35 350 

Fountain  Prairie.    T.  11,  R.  12  E. 

Marsh,  W.  hf .  Sec.  2 312 

Cent,  N.  W.  qr.  Sec.  2 370 

Mid.  S.  line  S.  W.  qr.  Sec.  6 400 

Mid.  S.  line  Sec.  6 340 


Fountain  Prairie.  T.  11,  R,  12  E.— (con.) 

Mid.  S.  hf.  of  N.  hf.  Sec.  7 370 

Mi.l.  W.  line  S.  W.  qr.  Sec.  8 370 

Mid.  S.  line  S.  W.  qr.  Sec.  8 360 

Mid.  S.  line  S.  W.  qr.  Sec.  9 350 

Mid  S.  line,  Sec.  9 330 

Stream,  S.  line  S.  W.  qr.  Sec,  10. ..  300 

Mid.  S.  line  Sec.  10 330 

Mid.  W.  hf.  Sec.  11 360 

Stream  crossing-,  N.  hf .  Sec.  14  ....  320 

Center  N.  E.  qr.  Sec.  13 314 

Mid.  W.  line  Sec.  28 350 

Mid.  E.  hf .  Sec.  29 360 

Stream,  S.  E.  cor.  Sec.  30 295 

^  mile  south 340 

S.  E.  cor.  Sec.  31 310 

Mid.  S.  line  S.  E.  qr.  Sec.  32 335 

Mid.  S.  line  Sec.  &3   295 

Mid.  S.  line  Sec.  34 280 

S.  E.  corner  Sec.  36  252 

Caledonia.    T.  11,  R.  8  E. 

Mid.  N.  W.  qr.  Sec.  3 360 

Mid.  S.  line  Sec.  7 480 

Mid.  S.  hf .  Sec.  8 510 

Center  S.  E.  qr.  Sec.  8 395 

Center  S.  E.  qr.  Sec.  9 520 

Mid.  S.  line  Sec  16 485 

Mid.  W.  line,  Sec.  16 385 

Mid.  W.  line  N.  W.  qr.  Sec.  21. ...  330 
Mid.  W.  line  Sec.  21 375 

Caledonia.    T.  12,  R.  8  E. 
Church,  N.W.qr.N. W.qr.Sec. 21.  280 

%  mile  south 420 

Mid.  S.  line  S.  W.  qr.  Sec.  22 500 

Mid.  N.  hf.  Sec.  25 205 

Cent.  N.  W.  qr.  Sec.  25 340 

Road,  W.  line  N.  W.  qr.  Sec.  25. ..  505 

Mid.  E.  hf.  Sec.  26 560 

Center  Sec.  26 560 

S.  E.  qr.  N.  E.  qr.  Sec.  26. 620 

Center  Sec.  27 510 

Stream  crossing,  S.  W.  qr.  Sec.  27 .  480 

Mid.  S.  line  S.  E.  qr.  Sec.  27 610 

Center  S.  E.  qr.  Sec.  28 470 

S.  W.  cor.  Sec.  28 440 

Mid.  S.  lineSec.29  360 

S.  W.  cor.  Sec.  29 420 

Mid.  N.  hf .  Sec.  29 580 

Mid.  W.  line  N.  W.  qr.  Sec.  29.     . .  505 

Center  N.  W.  qr.  Sec.  30 505 

Mid.  W.  line  N.  W.  qr.  Sec.  30. ...  540 

Bluff  top.  S.  E.  qr.  Sec.  34 760 

Mid.  S.  line  S.  W.  qr.  Sec.  35 310 

Caledonia.    T.  12,  R.  9  E. 
Bridge,  Sec.  7 2LX) 

Wyoeena.    T.  12,  R.  10  E. 

Railroad,  W.  line  Sec.  1 235 

Mid.  W.  line  Sec.  10 225 

S.  W.  cor.  Sec.  10 240 

Center  Sec.  12 230 

Stream,  S.  line  Sec.  12 215 

Center  Sec.  13 260 

Mid.  W.  line  Sec.  13 275 

Stream,  center  Sec.  14 210 

Center  Sec.  15 250 


444 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


BAROMETRICAL  ALTITUDES  —  continued. 


Wyocena.    T.  12,  R.  10  E.  —  (con.) 

Mid.  W.  line  Sec.  15 230 

Wyocena  depot 240 

Center  Sec.  28 280 

Mid.  W.  line  Sec.  28 310 

Mid.  E.  hf.  Sec.  29 275 

S.  W.  cor.  Sec.  29 320 

Mid.  E.  hf.  Sec.  31 280 

Mid.  W.  hf .  Sec.  31 235 

Mid.  W.  line  N.  W.  qr.  Sec.  36- ...  290 
Springvale.    T.  12,  R.  11  E. 
One-fourth  niile  N.  of  cent,  of  Sec.  1  235 

Mid.  E.  line  Sec.  1 240 

Mid.  W.  line  N.  W.  qr.  Sec.  2 280 

Mid.  N.  hf.  Sec.  3 290 

Mid.  W.  line  Sec.  4 235 

Railroad,  W.  line  Sec.  5  240 

S.  W.  cor.  Sec.  5 230 

Mid.  E.  hf.  Sec.  7 235 

Center  Sec.  7 230 

CenterSec.  15 360 

Mid.  W.  line  Sec.  15 360 

Bluff  top,  N.  E.  qr.  Sec.  16 370 

Mid.  E.  hf.  Sec.  17 300 

Stream  crossing,  N.  hf.  Sec.  18 222 

Stream  crossing,  N.  lif .  Sec.  22  ...     266 

Mid.  S.  hf.  Sec.  22 320 

Mid.  N.  hf .  Sec.  27 270 

Road,  W.  line  N.  W.  qr.  Sec.  27. ..  260 

Mid.  S.  line  S.  E.  qr.  Sec.  28 280 

Mid.  S.  line  Sec.  28 300 

S.  W.  cor.  Sec.  28 290 

Mid.  S.  hf.  Sec.  29 250 

S.  W.cor.  Sec.  29 300 

Mid.  S.  line  S.  W.  qr.  Sec.  29 280 

Courtland.    T.  12,  R.  12  E. 

Randolph  depot,  Sec.  1 378 

S.  E.  cor.  Sec.  1 360 

Mid.  N.  hf .  Sec.  2 365 

Center  Sec.  2 355 

Mid.  W.  line  Sec.  2 375 

Mid.  W.  hf .  Sec.  3 355 

Mid.  N.  line  N.  W.  qr.  Sec.  3    ....  355 

Mid.  N.  line  N.  E.  qr.  Sec.  4 355 

Mid.  N.  line  N.  W.  qr.  Sec.  4 325 

Mid.  S.  line  S.  W.  qr.  Sec.  5 375 

Cambria  depot,  Sec.  6 284 

Mid  W.  hf .  Sec.  8 380 

S.  W  qr.  Sec.  8 390 

Center  N.  W.  qr.  Sec,  11 402 

Mid.  W.  hf.  Sec.  11 390 

S.  W.cor.  Sec.  11 383 

S.  W.  cor.  Sec.  13 377 

Mid.  S.  line  Sec.  14 364 

Mid.  W.  line  S.  W.  qr.  Sec.  14. ...  380 

Mid.  E.  line  N.  E.  qr.  Sec.  13 367 

Mid.  W.  hf.  Sec.  17 410 

Center  Sec.  19 430 

Mid.  S.  hf.  Sec.  19 350 

Mid.  W.  hf.  Sec.  20 390 

Mid.  N.  hf .  Sec.  23 360 

Stream  crossing,  N.  hf.  Sec.  26 335 

Mid.  S.  hf.  Sec.  26 357 

Mid.  N.  hf .  Sec.  30 400 

Mid.  S.  line  Sec.  30 360 


Conrtland.    T.  12,  R  12  E.  —  (con.) 

Mid.  S.  hf .  Sec.  31 360 

Mid.  N.  hf .  Sec.  35 369 

Mid.  S.  line  Sec.  35 : . .  370 

Lewiston.    T.  13,  R.  7  E. 
Lewiston  depot,  Sec.  26 231 

Lewiston.    T.  13,  R.  8  E. 

Mid.  N.  hf  of  S.  W.  qr.  Sec.  14 250 

Center  S.  W.  qr.  Sec.  23 220 

Mid.  W.  line  Sec.  25 240 

Mid.  N.  hf.  Sec.  36 230 

Center  S.  E.  qr.  Sec.  36 245 

Fort  Winnebago.    T.  13,  R.  9  E. 

Mid.  W.  hf.  Sec.  16 230 

Mid.  W.  line  S.  W.  qr.  Sec.  16 260 

S.  W.  cor.  Sec.  16 280 

Center  S.  E.  qr.  Sec.  19 300 

Mid.  S.  line  S.  E.  qr.  Sec.  19 250 

Mid.  S.  line  Sec.  20 260 

Mid.  W.  line  Sec.  21 240 

Coughlin's  quarry,  E.  hf.  Sec.  20. ..  350 

Center  N.  E.  qr.  Sec.  30 ...  240 

Mid.  E.  hf  Sec.  31 390 

Mid.  N.  hf.  Sec.  36 265 

Bluff-top,  N.  W.  qr.  Sec.  36 390 

Marcellon.    T.  13,  R.  10  E. 

N.  E.  cor.  Sec.  1 260 

Mid.  N.  line  N.  E.  qr.  Sec.  1 320 

N.  W.  cor.  Sec.  1 260 

Mid.  W.  line  Sec.  1 300 

Mid.  W.  line  N.  W.  qr.  Sec.  12 320 

Mid.  S.  line  N.  W.  qr.  Sec.  12 290 

Mid.  W.  line  N.  W.  qr.  Sec.  13. ...  270 
Center  S.  E.  qr.  N.  E.  qr.  Sec.  14. ..  285 
Center  N.  W.  qr.  S.  E.  qr.  Sec.  14. .  295 

Mid.  S.  hf.  S.  W.  qr.  Sec.  14 290 

Y&  mile  E.  S.  W.  cor.  Sec.  14 270 

Center  Sec.  16 370 

Mid.  S.  hf.  Sec.  16 340 

Mid.  S.  line  S.  E.  qr.  Sec.  16 350 

Mid.  S.  line  Sec.  16 350 

Mid.  E.  line  N.  E.  qr.  Sec.  21 355 

Mid.  E.  line  Sec.  21 305 

Center  S.  E.  qr.  S.  E.  qr.  Sec.  21  ...  335 
CenterS.  E.  qr.  N.  E.  qr.  Sec.  22. ..  320 

S.  W.  cor.  Sec.  23    350 

Mid.  S.  line  S.  W.  qr.  Sec  23 360 

Mid.  S.  line  Sec.  23 350 

Mid.  S.  line  Sec.  24 300 

Mid.  S.  line  S.  E  qr.  Sec.  24 290 

Mid.  E.  line  N.  W.  qr.  Sec.  25 350 

Center  N.  W  qr.  N.  E.  qr.  Sec.  28.  260 

Scott.    T.  13,  R.  11  E. 

YK  mile  E.  N.  W.  cor.  Sec.  2 390 

Mid.  N.  line  Sec.  2 360 

Mid.  N.  hf.Sec.  2 360 

Mid.  N.  line  N.  E.  qr.  Sec.  3 300 

N.  W.  cor.  Sec.  3 280 

Mid.  N.  line  N.  W.  qr.  of  N.  E.  qr. 

Sec.  4 280 

Mid.  N.  line  N.  W.  qr.  Sec.  4 260 

Mid.  N.  line  N.  E.  qr.  Sec.  5 320 

%  mile  E.  N.  W.  cor.  Sec.  5 260 

Mid.  N.  line  N.  E.  qr.  Sec.  6 280 

Mid.  N.  hf.  of  N.  hf.  Sec.  11 350 


SURFACE  RELIEFS. 


445 


BAROMETRICAL  ALTITUDES  —  continued. 


Scott.    T.  13,  R.  11  E.  —  (con.) 

Mid.  S.  line,  Sec.  11 340 

Mid.  N.  hf.  Sec.  14 385 

Mid.  N.  hf.  S.  hf.  Sec.  14 340 

Mid.  S.  line  Sec.  14 330 

Mid.  N.  line  S.  E.  qr.  S.  W.  qr.  Sec. 

14 370 

i\  mi.  north  S.  E.  cor.  Sec.  19 230 

Mid.  S.  line  Sec.  19 270 

Mid.  N.  hf.  N.  hf.  Sec.  23 290 

Mid.  S.  line  Sec.  23 370 

i  mi .  north  center  Sec.  26 380 

•Ar  mi.  south  N.  W.  cor.  Sec.  29. ...  230 

Mid.  W.  line  Sec.  29 240 

'S.  W.  cor.  Sec.  29  .. 325 

Mid.  E.  line  Sec.  31 400 

i  mi.  north  S.  E.  cor.  Sec.  31 375 

|  mi.  east  S.  W.  cor.  Sec.  32 350 

S.  E.  cor.  Sec.  32 440 

Mid.  S.  line  S.  E.  qr.  Sec.  33 380 

Mid.  S.  line  S.  W.  qr.  Sec.  34 275 

S.  E.  cor.  Sec.  34 400 

Mid.  S.  line  Sec.  35 420 

S.  E.  cor.  Sec.  35 425 

Mid.  S.  line  Sec.  36 420 

S.  E.  cor.  Sec.  36 400 

Randolph.    T.  13,  R.  12  E. 

N.  W.  cor.  Sec.  1 415 

Center  S.  E.  qr.  Sec.  1 320 

Mid.  N.  line  Sec.  2 420 

N.  W.  cor.  Sec.  2 250 

Mid.  W.  line  Sec.  2 370 

Mid.  N.  hf.  S.  hf.  Sec.  5 350 

Mid.  S.  line  Sec.  5 340 

Mid.  W.  line  Sec.  6 320 

S.  W.  cor.  Sec.  6 350 

Mid.  S.  line,  Sec.  7 420 

Mid.  W.  line  S.  W.  qr.  Sec.  7 320 

Mid.  N.  hf .  Sec.  8 350 

Mid.  S.  line  Sec.  8 360 

Mid.  E.  line  Sec.  9 365 

Mid.  E.  line  Sec.  11 395 

Center  Sec.  12 395 

S.  W.  cor.  Sec.  15 390 

Mid.  W.  line  Sec.  15 356 

Mid.  N.  hf.  N.  hf.  Sec.  16 356 

Mid.  N.  hf.  S.  hf.  Sec.  16 432 

Mid.  S.  line  Sec.  16 409 

Center  S.  E.  qr.  Sec.  17 400 

Center  N.  W.  qr.  Sec.  17 365 

Mid.  W.  line  S.  W.  qr.  Sec.  18 380 

Mid.  W.  line  N.  W.  qr.  Sec.  19. ...  400 

Mid.  N.  hf  N.  hf.  Sec.  20 400 

Center  S.  W.  qr.  Sec.  20 400 

Mid.  E.  line  S.  E.  qr.  Sec.  21 386 

Mid.  N.  hf.  N.  hf .  Sec.  24 350 

Center  S.  W.  qr.  S.  E.  qr.  Sec.  24. .  330 

Center  N.  E.  qr.  Sec.  25 3-^0 

Mid.  W.  line  Sec.  25 365 

Mid.  W.  line  Sec,  27 420 

Center  Sec.  28 353 

S.E.  cor.  Sec.  28 420 

Center  S.  E.  qr.  N.  W.  qr.  Sec.  29. .  360 

N.  W.  cor.  Sec.  30 440 

mile  N.  S.  W.  cor.  Sec.  30 400 


Randolph.    T.  13,  R.  12  E.  —(con.) 

Mid.  W.  line  N.  W.  qr.  Sec.  31. ...  350 

S.  W.  cor.  Sec.  31 240 

S.  E.  cor.  Sec.  31 260 

Center  S.  W.  qr.  N.  W.  qr.  Sec.  32,  390 

Mid.  S.  hf.  N.  W.  qr.  Sec.  32 382 

S.  E.  cor.  Sec.  36 360 

Spring  Green.    T.  8,  R.  4  E. 

Bluff,  N.  W.  qr.  Sec.  3,  base 144 

Bluff,  N.  W.  qr.  Sec.  3,  top 374 

Bluff,  N.  W.  qr.  Sec.  5,  base  ....  200 

Bluff,  N.  W.  qr.  Sec.  5,  summit  . . .  465 

Spring  Green  depot,  Sec.  7 144 

Spring  Green.    T.  9,  R.  4  E. 

Bluff  top,  N.  E.  qr.  Sec.  28. 430 

S.  E.  qr.  N.  W.  qr.  Sec.  30 460 

Road,  N.  W.  qr.  Sec.  31 360 

Bluff,  S.  E.  qr.  Sec.  32 320 

Stream,  S.  W.  qr .  N.  W.  qr.  Sec.  34  140 

Troy.    T.  8,  R."4  E. 

Bluff  base,  Sec.  1 170 

Bluff  top,  Sec.  1 420 

N.  W.  cor.  Sec.  2 130 

Troy.    T.  9,  R.  4  E. 

Road,  N.  W.  qr.  Sec.  24 185 

Bluff  top,  N.  W.  qr.  Sec.  24 375 

Mid.  N.  hf.  Sec.  25 270 

Mid.  W.  hf.  Sec.  25 440 

Mid.  W.  line  Sec.  25 270 

Stream  crossing,  S.  W.  qr.  Sec.  35  .  134 

Bluff  top,  S.  W.  qr.  N.  E.  qr.  Sec.  35,  370 

Troy.    T.  9,  R.  5  E. 

Mid.  N.  line  Sec.  8 180 

N.  E.  cor.  Sec.  8 160 

Road,  S.  W.  qr.  S.  W.  qr.  Sec.  11. .  330 
Bluff  base,  N..W.  qr.  N.  W.  qr.  Sec. 

14 210 

Bluff  top,  N.  W.  qr.  N.  W.  qr.  Sec.  14,  500 

Road,  S.  E.  qr.  S.  W.  qr.  Sec.  17. ..  170 

Bluff  top,  S.  E.  qr.  S.  W.  qr.  Sec.  17,  250 

Center  Sec.  17 170 

N.  line  N.  W.  qr.  Sec.  19 170 

N.  W.  cor.  Sec.  24 370 

Mid.  S.  hf.  S.  hf.  Sec.  35 190 

Bluff  base,  N.  hf.  Sec.  35 190 

Bluff  top,  N.  hf.  Sec.  35 410 

Prairie  du  Sac.    T.  9,  R.  6  E. 

Sauk  City,  Sec.  12 210 

Bluff  base,  N.  W.  qr.  Sec.  17 180 

Bluff  top,  N.  W.  qr.  Sec.  17 490 

Bluff  base,  S.  W.  qr.  Sec.  21 166 

Bluff  top,  S.  W.  qr.  Sec.  21 486 

Prairie  du  Sac.    T.  10,  R.  6  E. 

Mid.  E.  hf.  Sec.  25 250 

Center  Sec.  26 250 

Mid.  W.  line  Sec.  27 220 

Franklin.    T.  9,  R.  9  E. 

Mid.  S.  line  Sec.  2 195 

Road.  S.  E.  qr.  Sec.  9 220 

Road,  N.  E.  qr.  Sec.  18 250 

Road,  S.  W.  qr.  Sec.  18 320 

Road,  N.  W.  qr.  Sec.  19 465 

Mid.  W.  hf.  Sec.  19 490 

Franklin.    T.  10,  R.  4  E. 

Summit,  E.  line  Sec.  21 380 


446 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


BAROMETRICAL  ALTITUDES  —  continued. 


Frankliin.    T.  10,  R.  4  E.  —(con.) 

Mid.  S.  line  Sec.  29    250 

Honey  Creek.    T.  10,  R.  4  E. 

Center  Sec.  1 530 

Mid.  N.  line  Sec.  1 570 

Bluff-base,  Sec.  12 205 

Bluff-top,  Sec.  12 480 

Bluff-top,  N.  W.  qr.  Sec.  13 300 

Bluff-top,  N.  E.  qr.  Sec.  14 290 

Bluff-top,  Sec.  35 462 

Center  Sec.  36 250 

Honey  Creek.    T.  10,  R.  5  E. 

S.  E.  qr.  Sec.  2 610 

Oclisner's,  N.  W.  qr.  Sec.  31 200 

Sampler.    T.  10,  R.  6  E. 

Mid.  S.  line  Sec.  10 240 

Center  Sec.  15 250 

Stream  crossing,  W.  hf.  Sec.  15 230 

Bluff-top,  W.  hf.  Sec.  15 415 

Sumpter.    T.  11,  R.  6  E/ 

Mid.N.  line  Sec.  26 550 

Road,  N.  E.  qr.  S.  E.  qr.  Sec.  26. ..  575 
Road,  S.  E.  qr.  S.  E.  qr.  Sec,  26  ...  625 

Center  N.  W.  qr.  Sec.  27 600 

Center  Sec.  34 280 

Road,  N.  E.  qr.  N.  E.  qr.  Sec.  35  . .  480 
Mid.  S.  line  S.  E.  qr.  Sec.  35 320 

Merrimack.    T.  11,  R.  7  E. 
Ridge,  S.  W.  qr.  S.  E.  qr.  Sec.  19. .  471 

Center  N.  W.  qr.  Sec.  23 580 

Mid.  N.  line  N.  W.  qr.  Sec.  26  ....  295 

S.  hf.  N.  W.  qr.  Sec.  28 280 

Mid.  S.  E.  qr.  N.  E.  qr.  Sec.  28. ...  260 

Road,  N.  hf.  S.  E.  qr.  Sec.  31 285 

Mid.  N.  hf.  Sec.  32 290 

Under  bridge,  N.  E.  qr.  Sec.  32. ...  270 

Westfleld.    T.  11,  R.  4,  E. 

Mid.  E.  line  Sec.  1 497 

Center  Sec.  1  500 

Mid.  N.  line  Sec.  1 500 

S.  W.  cor.  Sec.  2 530 

Bluff- top,  center  Sec.  3 471 

CenterSec.il 610 

Mid.  S.  line  Sec.  11 660 

Center  N.  W.  qr.  Sec.  11 560 

N.  W.  cor.  Sec.  11 510 

Mid.  S.  hf.  Sec.  12 627 

Creek-crossing,  E.  hf.  Sec.  13 477 

W.  hf.  S.  W.  qr.  Sec.  13   650 

Center  Sec.  13 530 

Center  Sec.  14 650 

Logansville,  Sec.  17 330 

Center  N.  W.  qr.  Sec.  17 351 

Center  S.  W.  qr.  Sec.  17 361 

Bluff,  N.  line  Sec.  17 471 

S.  W.  cor.  Sec.  25 540 

Mid.  S.  line  Sec.  26 520 

Mid.  E.  line  N.  W.  qr.  Sec.  29 401 

S.  E.  qr.  S.  E.  qr.  Sec.  35 400 

Center  S.  W.  qr.  Sec.  36 580 

Freedom.    T.  11,  R.  5  E. 

Bridge,  E.  hf.  Sec.  2 268 

Bloom's  Station,  Sec.  2 280 

Mid.  N.  line  N.  W.  qr.  Sec.  5 437 

Mid.  W.  line  Sec.  14 340 


Freedom.    T.  11,  R.  5  E.  —  (con.) 

S.  hf.  Sec.  23 700 

Near  S.  E.  cor.  Sec.  23 830 

Mid.  E.  line  Sec.  26 830 

Bamboo.    T.  11,  R.  6  E. 

Baraboo  depot,  Sec.  2 280 

Mid.  S.  line  S.  E.  qr.  Sec.  11 325 

Mid.  E.  hf.  Sec.  23 635 

Railroad  at  Cliff  House,  Sec.  24. ...  386 

Bluff-top,  S.  E.  qr.  Sec.  24 805 

Bluff- base,  S.  E.  qr.  Sec.  24 390 

Cliff-top,  mid.  W.  line  Sec.  24 850 

Baraboo.    T.  12,  R.  6  E. 

Mid.  W.  hf  Sec.  25 430 

Mid.  E.  line  Sec.  25 380 

S.  W.  qr.  S.  E.  qr.  Sec.  27 420 

S.  W.  qr.  S.  E.  qr.  Sec.  28 310 

N.  E.  cor.  Sec.  35 400 

Mid.  N.  line  N.  W.  qr.  Sec.  36 370 

Greenfield.    T.  11,  R.  7  E. 

Summit,  S.  W.  qr.  Sec.  1 715 

Mid.  W.  line  Sec.  1 535 

Mid.  W.  line  N.  W.  qr.  Sec.  1 543 

Near  Mid.  S.  hf  Sec.  5 275 

Center  S.  E.  hf  Sec.  5 275 

Road-forks,  N.  line  N.  W.  qr.  Sec.  7  270 

Near  center  N.  hf  Sec.  14 740 

Near  center  Sec.  15 850 

Near  Mid.  W.  line  Sec.  15 900 

Road,  S.  hf  N.  E.  qr.  Sec.  16 845 

W.  line  Sec.  16 750 

Yz  mile  S.  center  Sec.  16 600 

Mid.  W.  hf  Sec.  17 610 

Greenfield.    T.  12,  R.  7  E. 

Quarry,  center  Sec.  25 410 

20  rods  N 425 

Road,  N.  line  N.  E.  qr.  Sec.  26  ....  215 

Bluff,  top  N.  line  N.  E.  qr.  Sec.  26.  515 

Mid.  W.  line  Sec,  27 325 

Mid.  W.  line  Sec.  29 405 

Mid.  E.  hf  Sec.  30 475 

Center  Sec.  30 405 

Mid.  E.  hf  Sec.  32 345 

Mid.  W.  hf  Sec.  32 275 

Center  Sec.  33 270 

N.  W.  cor.  Sec.  36 350 

N.  E.  cor.  Sec.  36 365 

Stream-crossing,  N.  W.  qr.  Sec.  36 .  345 

S.  W.  cor.  Sec.  36 465 

Reedsburg.    T.  12,  R.  4  E. 

Creek- crossing,  S.  line  Sec.  1 285 

Mid.  S.  line  Sec.  2 320 

S.  W.  cor.  Sec.  9 330 

Reedsburg  depot,  Sec.  10 296 

Mid.  E.  line  Sec.  17 320 

E.  hf  S.  E.  qr.  Sec.  20 340 

Mid.  S.  line  Sec.  20 500 

Mid.  W.  line  Sec.  22 451 

Mid.  N.  line  S.  E.  qr.  Sec,  25 3o2 

Center  Sec.  25 '.  302 

Mid.  S.  line  Sec.  25 807 

Mid.  S.  line  S.  W.  qr.  Sec.  26 '290 

Mid.  W.  hf  Sec.  29 550 

Quarry,  S.  W.  qr.  Sec.  29 330 

S.  E.  cor.  Sec.  29 3SO 


RELATIONS  OF  THE  TOP03RAPHY  TO  THE  GEOLOGY. 


BAROMETRICAL,  ALTITUDES  —  continued. 


Reedsburg.    T.  12,  R.  4  E.  —  (con.) 

Center  Sec.  30 580 

S  W.  cor.  Sec.  30 560 

Cross  roads,  N.  hf  Sec.  30 335 

Mid.  W.  line  Sec.  30 580 

Mid.  N.  line  N.  W.  qr.  Sec.  31. ...  500 

Creek  crossing,  Sec.  35 280 

Mid.  S.  hf  Sec.  36 467 

Mid.  S.  line  Sec.  36 517 

Center  Sec.  36 460 

Excelsior.    T.  12,  R.  5  E. 

Mid.  N.  hf  Sec.  2 290 

Mid.  S.  line  S.  W.  qr.  Sec.  3 325 

Mid.  S.  line  S.  W.  qr.  Sec.  4 365 

S.  W.  cor.  Sec.  5 320 

Bluff  top,  Mid.  E.  hf  E.  hf  Sec.  5  . .  575 

Center  Sec.  28 500 

Bluff  top  N.  E.  qr.N.  W.  qr.  Sec. 

31 507 

Ableman's  depot,  Sec.  33 297 

Fairfleld.    T.  12,  R.  7  E. 

Mid.  S.  line  Sec.  17 315 

Center  S.  E.  qr.  Sec.  17 230 

Mid.  W.  line  S.  W.  qr.  Sec.  19  ....  335 

Center  S.  W.  qr.  Sec.  20 340 

Center  N.  W.  qr.  Sec.  20 350 

Road,  mid.  E.  hf  Sec.  22 226 

Bluff  top,  %  mile  S 450 

Bluff  top.  E.  line  S.  E.  qr.  Sec.  22.     590 
Bridge,  center  Sec.  23 225 

Winfield.    T.  13.  R.  4  E. 

S.  W.  qr.  Sec.  24 372 

S.  E.  cor.  Sec.  24   468 

W.hf.Sec.27 413 

S.  E.  cor.  Sec.  27 286 

Mid.  W.  line  S.  W.  qr.  Sec.  33  ....  307 
Center  Sec.  35  408 

Dellona.     T  13,  R.  5  E. 

Mid.  N.  hf.  Sec.  5 300 

Center  N.  W.  qr.  Sec.  19 390 

Juneau  County. 

T.  14,  R.  2  E. 

Mid.  S.  line  Sec.  6 430 

Mid.  E.  hf .  Sec.  7 310 

Mid.  W.  hf .  W.  hf .  Sec.  24 550 

T.  14,  R.  5  E. 

High  crest,  Sec.  28  700 

T.  15,  R.  3  E. 

Mid.  S.  line  S.  E.  qr.  Sec.  7 360 

Bluff  Sec.  13,  base 300 

BluffSec.  13,  top  500 


Juneau  County  —  (con.) 

T  *17  R  2  E 

Target  bluff,' Sec.  28,  top 476 

Target  bluff,  Sec.  28,  base 356 

T  18  R  3  E 

Foot  of  bluff,  Ne'ced'ah 340 

Top  of  bluff,  Necedah  510 

T.  18,  R.  4E. 

Petenwell  peak,  Sec.  9,  top     530? 

Adams  County. 

T.  14,  R.  6  E. 

S.  E.  qr.  Sec.  21,  Eleph.  back,  top.  550 
Wis.  river  hf .  mile  west,  Sec.  21 240 

T.  17,  R.  6  E. 

Friendship  mound,  Sec.  6,  top 750 

Bridge  at  foot,  Sec.  6   440 

T.  7,  R.  7  E. 

N.  E.  qr.  Sec.  3.   Pilot  knob,  base. .  540 
N.  E.  qr.  Sec.  3,  Pilot  knop,  top  ...  705 
Marquette  County 

T.  14,  R.  8  E. 
E.  line  Sec.  12 235 

T.  14,  R.  9  E. 
Merrils1  S.  E.  qr.  N.  E.  qr.  Sec.  7  . .  196 

T.  14,  R.  10  E. 

Observ.  hill,  S.  E.  qr.,  Sec.  7  base  . .  240 
Observ.  Ml,  S.  E.  qr.,  Sec.  7  top  ...  490 

T.  17,  R.  8  E. 

N.  W.  qr.  Sec.  7,  lime  bluffs,  top  . .  730 
N.  W.  qr.  Sec.  7,  lime  bluffs,  base. .  570 
Portage  County. 

T.  21,  R.  8  E. 

Mosquito  bluff,  Sec,  23,  top 630 

Mosquito  bluff.  Sec.  23,  base   520 

Marathon  County. 

T  28  R   7  "R1 

Top  Rib  hill,' W.'  end,  W.  hf.  Sec.  8  1263 
Top  Rib  hill,  E.  end,  W.  hf.  Sec.  9  1143 
Lower  Mosinee  hill,  center  Sec.  27, 

top 880 

Lower  Mosinee  hill,  river  at  foot  . .  600 
Upper  Mosinee  hill,  N.  E.  qr.  Sec. 

27,  top 1030 

Upper  Mosinee  hill,  river  at  foot . .     600 

T.  29,  R.  7  E. 

Mid.  Kline  Sec.  1...     890 

Wausau  depot,  Sec.  36 643 

Jackson  County. 

T.  21,  R.  4  W. 

Isolated  bluff,  Sec.  23,  base 230 

Isolated  bluff,  Sec.  23,  top 489 


RELATIONS  OF  THE  TOPOGRAPHY  TO  THE  GEOLOGY  OF  THE  REGION. 

The  topography  of  all  countries  is  chiefly  dependent  upon  the  na- 
ture of  the  geological  formations  immediately  underlying  the  surface. 
This  is  markedly  so  in  Central  Wisconsin.  The  rock  systems  of  this 
portion  of  the  state  are  altogether  Archaean  and  Lower  Silurian;  the 
former  consisting  of  gneisses,  granites  and  schists,  with  other  crys- 
talline rocks,  the  latter  of  a  series  of  alternating  sandstones  and  lime- 


448  GEOLOGY  OF  CENTRAL  WISCONSIN. 

stones,  in  nearly  horizontal  beds.     These  include,  in  ascendino-  or- 
der, the  Potsdam,  or  Lower  sandstone,  the  Mendota  limestone,  the 
Madison  sandstone,  the  Lower  Magnesian  limestone,  the  St.  Peters 
sandstone,  the  Trenton  limestone,  and  the  Galena  limestone.     The 
last  named    covers  but  a  very  small  portion  of   our  district.     The 
Archaean  rocks  lie  in  a  great  central  mass  in  the  northern  part  of  the 
state,  the  Silurian  formations  encircling  this  mass  in  imbricatino-  or- 
der, and,  coming  to  the  surface  in  a  series  of  receding  concentric 
bands,  together  forming  the  southern,  eastern  and  western  parts  of 
the  state.     The  surface  features  of  the  Archaean  and  Silurian  regions 
differ  much.     In  the  Archaean  area  we  have  unquestionable  proof,  in 
the  crumpled  condition  of  the  rocks,  of  its  former  mountainous  char- 
acter.    Denudation  has  gradually,  in  the  great  lapse  of  time  during 
which  these  beds  have  been  exposed,  stripped  it  entirely  of  these  char- 
acteristics, leaving  it  now  merely  a  high,  and,  in  general,  a  gently  undu- 
lating area,  broken  only  very  occasionally  by  small  isolated  ridges  or 
peaks  of  quartzose  rocks,  which  have  remained  standing  by  virtue 
of  their  superior  hardness  and  power  of  resisting  chemical  action.     In 
minor  detail,  however,  the  Archaean  area  is  much  roughened  by  low 
ridges  whose  sides  frequently  show  outcropping  ledges  of  tilted  rock. 
In  the  Silurian  area,  on  the  other  hand,  the  original  condition  must 
have  been  a  nearly  level  one,  and  denudation  has  worked  here  in  an  op- 
posite direction,  removing  great  portions  of  the  horizontal  beds,  goug- 
ing them  everywhere  into  valleys,  and  producing  thus  narrow  ridges 
and  bold  isolated  bluffs.     The  horizontality  of  the  Silurian  strata,  which 
is  more  nearly  exact  in  central  Wisconsin  than  elsewhere  in  the  state, 
together  with  their  alternately  hard  and  soft  characters,  has  resulted 
in  producing  a  peculiar,  abruptly  roughened  surface  —  narrow  valleys 
with  abrupt,  bluffy  sides,  and  irregular  table-like  outliers. 

These  peculiarities  of  topography,  resulting  from  the  different  ef- 
fects of  the  eroding  agencies  on  the  different  kinds  of  rocks,  have, 
however,  in  a  large  portion  of  the  region,  been  much  modified  and 
obscured  by  other  causes.  I  refer  to  those  causes  which  gave  rise 
to  the  glacial  drift.  The  southwestern  quarter  of  the  state  of  Wis- 
consin is  without  trace  of  the  glacial  depositions,  whilst  all  of  the 
rest  of  the  state  is  characterized  by  the  presence  of  unusually  large 
quantities  of  these  materials.  The  line  of  demarkation,  moreover, 
between  the  drift-bearing  and  driftless  areas,  is  a  sharp  and  easily 
traced  one.  Entering  the  state  from  the  south  on  the  southern  line 
of  Green  county,  the  drift  limit  traverses  this  county  centrally  from 
south  to  north,  and  continues  northward  through  western  Dane  and 
central  Sank;  then,  curving  eastward  across  the  southern  end  of  Adams, 


VEGETATION  AND  SOILS.  449 

it  follows  along  the  eastern  line  of  that  county,  passes  into  Portage, 
curves  westward,  and  crossing  the  Wisconsin  river  again,  continues 
in  a  nearly  westward  direction  across  Wood,  Clark,  Jackson,  Trem- 
pealeau  and  Buffalo  counties,  to  about  the  foot  of  Lake  Pepin,  on  the 
Mississippi.  The  driftless  region  is  thus  nearly  altogether  within  the 
Silurian  area.  North  and  east  of  the  drift  limit  the  general  contours 
are  usually  flowing,  the  valleys  frequently  wide  and  ill  defined,  the 
rock  exposures  not  frequent,  and  the  outliers  not  many  in  number,  be- 
ing usually  of  large  size  and  without  jagged  edges  or  peaks.  On  the 
other  side  of  this  line  the  topography  is  strikingly  different;  the 
changes  of  level  are  abrupt,  the  valleys  narrow,  with  steep  and  high 
sides,  the  rock  exposures  frequent,  and  the  outliers  often  of  very  small 
dimensions  horizontally,  though  of  very  considerable  height,  and  of- 
ten showing  precipitous  sides  with  jagged,  peak-like  summits,  even 
when  of  soft  sandstone.  The  drift  forces  have  contributed  to  this  re- 
sult in  two  ways;  (I)  by  planing  down  the  irregularities  resulting 
from  subaerial  erosions,  and  (2)  by  the  deposition  of  great  quantities 
of  clay,  sand  and  gravel.  The  peculiar  mode  of  deposition  of  this 
material  has,  however,  itself,  in  much  of  the  region,  produced  a  pe- 
culiar irregularity  of  surface,  leaving  it  covered  with  ridges  of  low 
rounded  knobs,  and  intervening  rounded  depressions,  which  are  fre- 
quently filled  by  small  ponds  or  lakes.  It  is  also  true  that  the  change 
of  topography  noted  in  passing  from  the  driftless  to  the  drift-bearing 
area  is  not  exclusively  due  to  the  former  presence  or  absence  of  the 
glacial  forces,  but  is  in  some  measure  owing  to  the  fact  that  for  a 
long  distance  the  drift  limit  is  nearly  on  the  line  of  a  change  from  a 
horizontal  position  of  the  strata  to  a  gradually  increasing  eastward 
slope. 

A  much  closer  connection  can  be  traced  between  the  variations  in 
surface  features  and  the  changes  in  the  formations,  which  will  receive 
attention  hereafter. 

VEGETATION  AND  SOILS. 

These  are  noticed  here  only  in  their  most  general  relations;  the 
soils  only  in  reference  to  their  connection  with  the  underlying  geo- 
logical formations. 

The  three  different  kinds  of  surface  in  the  district,  as  to  vegetation, 

'  O  ' 

are  the  prairies,  marshes  and  timber  land.  The  prairies,  or  tree- 
less areas,  are  restricted  to  the  Silurian  region,  and  are  chiefly  charac- 
teristic, in  central  Wisconsin  at  least,  of  limestone  districts,  though 
occurring  also  on  the  sandstone  formations.  In  many  places  regions 
Wis.  SUR.  —  29 


4:50  GEOLOGY  OF  CENTRAL  WISCONSIN. 

once  prairie  have  been  invaded  by  a  timber  growth,  which  has  come 
in  since  the  settlement  of  the  country,  having  been  in  former  times 
checked  by  the  annual  prairie  fire's.  Very  large  areas  in  Adams 
county,  for  instance,  which  are  now  covered  with  a  thick  growth  of 
small  oaks,  are  said  to  have  been  open  prairies  at  the  time  of  the  first 
settlements.  The  prairie  areas  are  by  no  means  always  flat;  indeed, 
the  flat  prairies  are  the  exception,  and  have  chiefly  been  noticed  along 
the  bottom  land  of  the  Wisconsin  river.  The  ordinary  prairie,  how- 
ever, as  in  northern  Dane  and  eastern  Columbia  county,  is  very  roll- 
ing, commonly  showing  abrupt  changes  of  level,  even  up  to  fifty  or 
a  hundred  feet.  These  changes  in  level  are,  in  places,  due  to  heaped 
up  drift,  but  more  commonly  to  unequal  denudation  of  the  rocky 
strata.  In  many  cases,  as,  for  instance,  in  the  town  of  West  Point, 
Columbia  county,  the  prairie  area  includes  both  lowland  and  bold 
outlying  bluffs,  as  much  as  two  hundred  or  even  three  hundred  feet 
in  height.  The  Central  Wisconsin  prairies  are,  with  one  notable  ex- 
ception, of  small  size,  occupying  at  most  not  more  than  two  or  three 
sections.  The  exception  is  the  limestone  prairie  belt  which  occupies 
large  portions  of  the  towns  of  Springfield,  Westport,  Dane,  Vienna, 
Windsor  and  Bristol,  in  northern  Dane  county;  and  of  West  Point, 
Lodi,  Arlington,  Leeds,  Hampden  and  Lowville,  in  Columbia  county. 
The  same  belt,  though  somevvhat  broken  in  the  towns  of  Otsego  and 
Courtland,  continues  to  the  northeast  and  passes  into  Green  Lake 
county.  This  large  prairie  area  is  for  the  most  part  on  high  land, 
occupying  the  summit  of  the  watershed  between  the  Wisconsin  and 
Rock  rivers.  It  is  nearly  always  underlaid  by  the  Lower  Magnesian 
limestone,  whose  irregular  upper  surface  contributes  much  to  the 
rolling  character  of  the  prairie. 

The  marshes  are  widely  scattered,  occurring  over  both  the  Archsean 
and  Silurian  areas,  though  more  numerously  in  the  former.  As  a 
general  rule  they  are  small,  but  in  some  cases  are  of  very  considerable 
size,  as,  for  instance,  those  extending  along  Duck  creek  and  the  up- 
per Fox  river  east  of  Portage,  which  are  many  miles  in  length,  and  the 
great  marsh  south  of  Plover,  in  Portage  county,  which  covers  the 
greater  part  of  four  townships.  Many  of  these  marshes,  as,  for  in- 
stance, the  Plover  marsh  just  alluded  to,  are  underlaid  by  a  valuable 
quality  of  peat. 

With  regard  to  timber,  it  may  be  said  that  all  of  the  counties  of 
Dane,  Columbia,  Sauk  (except  on  the  quartzite  bluffs),  Juneau, 
Adams,  Marquette  and  Waushara  (except  on  the  east),  are  covered 
by  a  prevailing  growth  of  small  oaks;  whilst  Marathon,  Portage, 
eastern  Waushara,  most  of  Wood,  Clark,  and  much  of  Jackson,  are 


VEGETATION  AND  SOILS.  451 

heavily  timbered  with  pine  interspersed  with  hardwood  on  the  more 
elevated  lands.  The  Archaean  region  is  generally  heavily  timbered, 
north  Wisconsin  being  one  of  the  great  lumbering  districts  of  the 
continent. 

Geologically,  we  may  distinguish  the  drift,  the  purely  sandstone, 
the  purely  limestone,  and  the  crystalline  rock  soils.      The  last  three 
terms  are  meant  to  apply  to  such  soils  as  result  exclusively  from  the 
disintegration  of  the  underlying  rocky  formations.    Inasmuch  as  these 
formations  are  not  always  perfectly  pure  limestone  or  sandstone,  their 
disintegration  gives  other  ingredients  to  the  soil  than  lime  or  sand. 
The  drift  soils  are  either  bad  or  good  as  the  material  is  more  largely 
sandy,  or  shows  a  predominating  admixture  of  clayey  and  calcareous 
substances;  those  resulting  solely  from  the  disintegration  of  the  sand- 
stone, of  the'  poorest  quality;  whilst  the  limestone  soils  are  usually 
the  best  in  the  region.     The  crystalline  rock  soils  are  often  good,  but 
as  the  region  of  crystalline  rocks  is  nearly  everywhere  invaded  by  the 
drift,  its  soils  are  commonly  dependent  upon  the  nature  of  the  drift, 
rather  than  upon  that  of  the  subjacent  rock.     In  some  portions  of  the 
Archaean  region,  where  either  the  drift  is  not  present  in  very  large 
quantity,  and  the  felspathic  rocks  have  disintegrated  into  a  good 
clayey  soil,  as  in  the  high  land   in  the   western  part   of  Marathon 
county,  or  where  the  drift  is  itself  of  a  non-arenaceous  character, -as  in 
much  of  Clark  county,  and  in  many  places  along  the  line  of  the  Wis- 
consin   Central  Railroad,  excellent  lands  for  farming   are   made  by 
clearing  the  heavy  growths  of  hardwood  timber.     Where  the  drift  is 
more  sandy,  as  in  a  large  region  about  the  headwaters  of  the  Wiscon- 
sin  river,  the  land   is  worthless   for  agricultural  purposes,  though 
frequently  covered  with   a  valuable  growth  of  pine.     Through  the 
sandy  nature  of  the  drift  materials  the  sand  region  of  central  Wiscon- 
sin extends  in  places  far  beyond  the  district  occupied  by  the  Potsdam 
sandstone.  In  all  of  the  region  in  which  the  last  named  rock  is  the  sur- 
face formation,  and  where  the   drift  is    either  absent,  or  present  in 
small  quantities  only,  or  is  altogether  sandy  in  nature,  as  in  most  of 
Adams,  Juneau,  Sauk,  Jackson,  Marquette,  and  Waushara  counties, 
in  much  of  Columbia,  and  in  places  all  along  the  valley  of  the  Lower 
Wisconsin,  the  soil  is  generally  a  loose  sand,  and  the  land  of  the 
poorest  quality.     Where  the  drift   overlies    the  sandstone  and  con- 
tributes clayey  or  calcareous  matter,  as  in  the  southern  part  of  Adams 
county,  or  the  eastern  part  of  Waushara,  the  land  is  often  good.     In 
other  cases,  a  good  soil  within  the  Potsdam  area  and  where  the  drift 
is  absent  seems  to  have  resulted  from  the  filling  of  valleys  with  fine 
stream  detritus,  as  along  the  valley  of  the  Wisconsin;  or  from  the 


452  GEOLOGY  OF  CENTRAL  WISCONSIN. 

nearness  to  the  surface  of  certain  clayey  layers  included  within  the 
sandstone,  as  in  the  town  of  Reedsburg,  Sauk  county;  or  from  the 
presence  of  considerable  dolomitic  ^material  in  the  sandstone,  as  in 
the  town  of  Honey  Creek,  Sauk  county.  All  of  these,  are,  however, 
but  exceptions  to  the  general  rule,  that,  for  the  most  part,  the  Pots- 
dam area,  on  both  sides  of  the  drift  limit,  is  a  barren  sandy  region. 

Above  the  lowest  sandstone,  we  find,  first,  a  layer  thirty  feet  in 
thickness  of  clayey  or  sandy  dolomitic  limestone,  to  which  I  have 
given  the  name  of  Mendota  limestone.  Where  it  is  the  surface 
rock,  as  in  portions  of  the  towns  of  Scott  and  Marcellon,  Co- 
lumbia county,  a  good  clay  soil  usually  results.  Next  above  the 
Mendota  is  again  a  layer  of  sandstone,  which  I  will  designate  as  the 
Madison  sandstone,  having  a  thickness  of  30  to  40  feet.  Where  it  is 
the  surface  rock,  as  in  a  large  part  of  the  town  of  Otsego,  Columbia 
county,  the  soil  is  a  loose  sand,  and  of  little  value.  These  rapid  al- 
ternations explain  the  change  of  soil  noticed  with  a  slight  change  of 
elevation  in  many  places  along  the  borders  of  the  areas  occupied  by 
the  Lower  Magnesian  limestone,  which  is  the  next  formation  in 
order. 

The  Lower  Magnesian  is  a  great  mass  of  dolomitic  limestone,  80 
to  200  feet  in  thickness,  often  carrying  much  silicious  and  clayey 
matter  in  its  composition.  The  country  occupied  by  it  is  hence 
nearly  always  one  of  most  excellent  soils.  Such  is  the  soil  of  the  high 
prairie  belt  of  northern  Dane  and  eastern  Columbia.  These  prairies 
are  often  much  covered  with  drift,  which  occasionally  lends  a  sandy 
character  to  the  soil,  but  not  frequently,  since  the  drift  of  this  partic- 
ular district  itself  is  commonly  calcareous  and  clayey. 

The  next  rock  above  the  Lower  Magnesian,  the  St.  Peters  sand- 
stone, but  rarely  forms  the  surface  rock,  being  generally  concealed, 
when  present,  by  overlying  beds,  and  showing  only  on  hill-sides  and 
steep  slopes.  Where,  however,  it  comes  to  the  surface,  as  in  the  val- 
ley of  Sugar  river  in  western  Dane  county,  and  the  drift  is  absent, 
the  same  sandy  soil  is  observed  as  that  produced  by  the  disintegra- 
tion of  the  Lower  sandstone. 

The  Trenton  limestone  soils  are  usually  of  excellent  quality,  and 
frequently  somewhat  more  argillaceous  and  less  dolomitic  than  those 
from  the  Lower  Magnesian.  The  Galena  is  so  unimportant  a  forma- 
tion inCentral  Wisconsin  that  it  need  not  be  especially  alluded  to  in 
this  connection. 


MAP    OF 

CENTRAL.  WI  S  C 


HTDROGRAPHIC  BASINS  and  the  principal  TOPOORAPHICAL  SUBDIVISIONS 
R.  D.  Irving,  18V  (i. 


_  FRIENDSHIP  f\ 

ADAMtS/ 

//  LMARQ^T 


^^  _^_  Lit  nit  of Hyidrogmphic Basins 

tfortltern  andEeuttrnLimits  of 

DriftlfitArea 


,  ,  ~,,   ^          <&^m 

r<«— •       •/-  ••  »         ••''  -iy 
^•^          -       V    "    \       .-•'     j         •    .   -  *r 


The  Oysfaliine  rock  District 
The  Sandstone  District 
Thf  Limestone  Dist  rirt 


TOPOGRAPHICAL  SUBDIVISIONS.  453 

TOPOGRAPHICAL  SUBDIVISIONS  —  RESUME. 

The  foregoing  details,  with  regard  to  the  surface  slopes,  river 
systems,  surface  reliefs,  prairies,  marshes,  timber,  etc.,  of  central 
Wisconsin,  will  serve  to  render  intelligible  to  the  reader  a  very 
brief  summary  of  the  topographical  features  of  the  whole  dis- 
trict. 

First,  then,  we  find  on  the  north,  occupying  all  of  Marathon  and 
most  of  Portage,  Wood,  and  Clark  counties,  a  comparatively  elevated 
region  of  crystalline  rocks,  which  descends  gradually  from  an 
altitude  of  900  feet  on  the  north,  to  one  of  400  to  500  feet  on  the 
south.  In  general,  this  section  has  a  gently  undulating  surface, 
which  is,  however,  often  broken  in  minor  detail  by  low,  abrupt  ridges 
with  outcropping  tilted  rock  ledges,  and  is  dotted  occasionally  with 
high  points  of  quartzose  rocks.  The  whole  area  is  densely  covered 
with  a  forest  of  pine  interspersed  with  marshes,  and  hardwood  ridges, 
which  when  cleared  yield  excellent  land.  It  is  traversed  from  north 
to  south  by  two  large  rivers,  the  Wisconsin  on  the  east,  and  the 
Black  on  the  west,  which,  as  also  their  numerous  branches,  are 
rapid  streams,  broken  constantly  by  chutes  and  water  falls  over  tilted 
rock  ledges;  and  is  covered  everywhere  with  accummulations  of  drift 
material,  which  are,  however,  much  greater  in  some  places  than  in 
others. 

Proceeding  now  further  southward  we  come  next  upon  the  great 
central  sandstone  region  of  the  state.  This  covers  all  of  Jackson, 
Juneau,  Adams,  Marquette  and  Waushara  counties,  southern  Wood, 
Portage  and  Clark,  northern  and  western  Columbia,  and  most  of 

G  '  ' 

Sank.  It  extends  east  and  west  about  eighty  miles,  north  and  south 
about  one  hundred,  and  really  includes  several  subordinate  areas, 
which  are,  in  some  respects,  topographically  distinct,  but  all  of  which 
have  in  common  the  basement  rock  of  sandstone,  and,  for  the  most 
part,  the  sandy  soil.  For  the  greater  part  of  its  area,  the  sandstone 
district  is  out  of  the  heavy  timber,  which,  however,  invades  it  in  east- 
ern Waushara,  in  southern  Portage  and  Wood,  and  in  eastern  Jack- 
son. For  the  rest  of  the  district,  the  prevailing  growth,  except  on 
the  high  Archaean  bluffs  of  Sank,  is  of  small  oaks. 

Of  the  subordinate  areas,  we  note  first  on  the  east  a  district  (1), 
including  Waushara,  southern  Portage,  those  portions  of  Marquette 
and  Green  Lake  which  lie  north  of  the  Fox  river,  and  southern 
Adams,  which  is  everywhere  heavily  covered  with  glacial  drift,  to 
whose  irregular  morainic  method  of  deposition  is  to  be  attributed  a 
peculiar  roughened  surface,  dotted  in  places  with  small  lakes  that  oc- 


454  GEOLOGY  OF  CENTRAL  WISCONSIN. 

cupy  the  drift  depressions.  The  streams  of  this  region  are  numerous, 
large,  rapid,  and  extraordinarily  clear,  but  without  rock  rapids.  Rock 
bluffs  are  not  frequent,  and  those  that  occur  are  without  the  castel- 
lated appearance  so  characteristic  of  the  more  western  outliers.  The 
whole  of  the  area  descends  from  its  highest  parts  in  northwestern 
Waushara,  wrhere  the  altitude  is  about  540  feet,  in  a  southeasterly 
direction  towards  the  Fox  river,  whose  altitude  at  Portage  is  200 
feet,  and  at  Berlin  175  feet.  The  soil  of  this  district  is  for  the  most 
part  sandy.  In  central  Waushara,  however,  good  land  occurs  on 
limestone  and  crystalline  rock  drift,  whilst  in  eastern  Waushara  the 
stratified  drift  clays  yield  an  excellent  soil.  West  of  the  high 
ground  along  the  line  of  Adams  and  Waushara  counties,  we 
come  upon  an  altogether  different  region,  (2)  the  next  of  our  sub- 
ordinate divisions.  This  is  the  central  sand  plain  of  Adams  and 
Juneau  counties,  which  is  traversed  from  north  to  south  by  the  Wis- 
consin river.  Here  we  find  no  drift  at  all,  a  generally  flat  surface, 
rising  gradually  from  the  river  in  each  direction,  and  dotted  by  nu- 
merous lofty  and  jagged  peaks  of  sandstone,  large  and  clear  streams, 
and  a  prevailing  growth  of  small  oaks,  interrupted  by  a  few  prairies 
and  marshes,  and  mingling  writh  small  pine  towards  the  north. 
Crossing  now  the  divide  on  the  northwest  corner  of  Juneau  county, 
we  find  ourselves  in  the  sandstone  portion  of  the  Black  river  valley,  (3) 
which  resembles,  for  short  distances  from  the  river,  in  its  general 
sandy,  plain-like  character,  and  gigantic,  castellated  outliers,  the  re- 
gion last  described.  As  we  pass  westward,  however,  from  Black 
river,  or  southward  along  its  course,  we  find  ourselves  in  a  region  of 
narrow  but  deeply  eroded  valleys  and  of  steep  hills.  Returning  now 
to  the  central  plain  of  Juneau  county,,  and  proceeding  towards  its  south- 
west corner,  we  cross,  in  the  towns  of  Summit,  Wonewoc,  Plymouth  and 
Lindina,  a  high,  narrow,  and  deeply  indented  watershed,  and  find  our- 
selves in  the  upper  part  of  the  Baraboo  river  valley,  (4)  which  we  may 
regard  as  another  of  the  subordinate  districts  of  the  central  sandstone 

O 

region.  The  upper  part  of  this  valley  shows  the  usual  characters  of 
the  valleys  of  the  driftless  part  of  the  state,  being  narrow,  with  abrupt 
sides,  which  are  often  of  precipitous  sandstone.  The  tributary 
streams  have  similar,  but  narrower  and  steeper  valleys.  On  either 
side  the  country  rises  rapidly,  and  shows  frequently  excellent  land. 
As  the  river  is  followed  into  Sauk  county,  its  valley  widens,  but  the 
same  deeply  indented  divides  are  observed;  that  on  the  south,  in  the 
towns  of  Westfield  and  Reedsburg,  rising  into  the  horizon  of  the 
Lower  Magnesian  limestone,  so  that  large  patches  of  good  limestone 
country  occur  here.  In  central  Sauk  county  the  Baraboo  traverses 


TOPOGRAPHICAL  SUBDIVISIONS.  455 

the  length  of  the  valley  between  the  two  quartzite  ranges,  whose  top- 
ography has  already  been  sufficiently  indicated.  About  midway  in. 
the  east  and  west  length  of  this  valley  the  western  limit  of  the  gla- 
cial drift  is  met  with,  which  is  here  in  a  morainic  condition.  Cross- 
ing now  to  that  portion  of  Sauk  county  which  lies  to  the  south  of  the 
limestone-capped  divide  in  the  towns  of  Westfield  and  Franklin,  and 
of  the  southern  quartzite  range,  we  reach  a  part  of  the  valley  of  the 
Wisconsin  itself,  which  may  be  designated  as  the  Honey  Creek  dis- 
trict (5).  On  the  west  side  of  this  triangular  area  we  find  deeply 
eroded  valleys  with  limestone-capped  separating  ridges;  further 
south  and  east  towards  the  river,  numerous  outliers  and  peculiar  nar- 
row ridges  are  seen;  farther  east  still  these  cease  suddenly,  and  on 
the  wide  prairie  in  the  towns  of  Prairie  du  Sac  and  Sumpter,  morainic 
drift  begins  as  suddenly  again.  Along  the  Wisconsin  in  the  south- 
west corner  of  this  area,  the  limestone-capped  bluffs  of  an  immense 
outlier  bound  the  river  bottom  for  a  number  of  miles.  We  have  yet 
to  consider  the  last  of  these  subordinate  areas,  (6)  which  includes 
that  portion  of  Marquette  county  south  of  the  Fox  river,  and  the 
northern,  central  and  western  towns  of  Columbia  county,  being  lim- 
ited on  the  east  and  south  by  the  western  face  of  the  limestone  divide 
between  the  Wisconsin  and  Rock  rivers.  This  is  an  area  in  general 
level,  having  an  elevation  of  about  250  feet,  with  many  bold  lime- 
stone outliers.  It  is  drift  covered,  showing  numerous  large  bowlders, 
has  everywhere  a  sandy  soil,  and  a  somewhat  sparse  growth  of  small 
oaks. 

The  third  and  last  of  the  great  topographical  subdivisions  of  Cen- 
tral Wisconsin  we  may  designate  as  the  limestone  district,  since  in 
it  one  or  other  of  the  Silurian  limestones  is  almost  always  the  surface 
rock.  It  includes  eastern  and  southern  Columbia,  and  all  of  Dane,  is 
characterized  nearly  everywhere  by  an  excellent  soil,  includes  the 
largest  prairie  areas  of  central  Wisconsin,  shows  a  prevailing  growth 
of  oak,  and  has  a  rolling  and  diversified  surface.  The  drift  materials 
are  everywhere  present,  except  in  the  southwestern  towns  of  Dane, 
which  show  the  usual  abrupt  topography  of  the  driftfess  area.  On 
the  northern  side  of  this  district,  in  the  towns  of  Scott,  Randolph,  Court- 
land,  Otsego,  Lowville,  Hampden,  Leeds  and  Arlington,  in  Columbia 
county,  and  of  Vienna,  Westport,  Dane,  Springfield  and  Middleton, 
in  Dane  county,  there  is  a  nearly  continuous  belt  of  high  rolling  prai- 
rie from  about  400  to  600  feet  in  altitude.  The  underlying  rock  on 
this  prairie  is  limestone,  and  the  soil  of  the  very  best  quality.  From 
the  east  and  south  flanks  of  this  high  land  the  country  descends 
rapidly,  and  is  watered  by  the  various  head  streams  of  Rock  river. 


456  GEOLOGY  OF  CENTRAL  WISCONSIN. 

In  western  Dane,  the  descent  is  almost  entirely  towards  the  south, 
but  in  the  center  of  the  county  the  dip  of  the  strata  begins  to  veer 
eastward,  and  the  surface  slope  corresponds.  On  the  west  side  of  this 
county,  again,  in  the  valley  of  Sugar  river,  the  topography  is  more 
abrupt  than  elsewhere,  owing  to  the  entire  absence  of  the  drift  ma- 
terials; in  the  center  we  find  the  broad  southeast  valley  of  the  Catfish, 
with  its  chain  01  lakes  lying  in  N.  E. -S.  "W.  valleys,  and  its  morainic 
glacial  drift;  wThilst  further  east  still  we  find  a  more  nearly  level 
drift-covered  region,  sloping  gradually  eastward. 


GENERAL  GEOLOGICAL  STRUCTURE.  457 


CHAPTER  II. 

GENERAL  GEOLOGICAL  STRUCTURE  OF  CENTRAL 
WISCONSIN. 

The  region  of  country  included  within  the  boundaries  of  the  state 
of  Wisconsin  is  quite  simple  as  to  the  grand  features  of  its  rock 
structure,  and  may  be  briefly  described  as  consisting  of  a  great  nucle- 
us of  ancient  crystalline  rocks,  encircling  which,  but  more  especially 
on  the  east,  south,  and  west,  are  succeeding  bands  of  limestone  and 
sandstone,  belonging  to  the  Silurian  series. 

Forming  most  of  the  northern  half  of  the  state  is  a  great  mass  of 
crystalline  rocks  —  granites,  gneisses,  chloritic  micaceous  and  horn- 
blendic  schists  being  the  predominating  kinds  —  which  are  folded 
and  eroded  so  as  to  offer  the  greatest  obstacles  to  their  detailed  study, 
and  which  appear,  for  the  most  part,  to  be  referable  to  the  Laurentian 
division  of  the  Archaean. 

On  the  northern  edge  of  this  central  nucleus,  just  south  of  Lake 
Superior,  in  Bayfield  and  Ashland  counties,  is  a  narrow  belt  of  quartz- 
ites,  magnetic  and  specular  iron  ores,  diorites,  talcose  chloritic  and 
black  slates,  etc.,  which  overlie  unconforrnably  the  gneisses  of  the 
Laurentian  immediately  to  the  south.  This  fact,  taken  together  with 
their  nature  and  relations  to  the  newer  adjoining  formations,  would 
seem  to  throw  these  beds,  without  any  doubt,  into  the  same  catagory 
with  the  Iron  Bearing  series  of  Michigan,  and  the  Huronian  system 
of  Canada.  Similar  rocks,  with  similar  relations  to  the  surrounding 
formations,  exist  in  Oconto  county,  on  the  northeast  border  of  the 
state,  from  where  they  stretch  far  into  the  Upper  Peninsula  of  Michi- 
gan, and  include  the  famous  iron  regions  of  Marquette  and  the  Me- 
nomonee.  On  the  south  side  of  the  Laurentian  core,  on  Black  river, 
in  Jackson  county,  are  again  similar  rocks,  whose  Huronian  age  is 
not  so  clearly  made  out.  Still  farther  'south,  and  within  the  area  of 
the  Silurian  formations,  are  projecting  portions  of  the  here  buried 
Archaean.  These  isolated  masses  are  made  up  chiefly  of  quartzites 
and  dark-colored  quartz-porphyries,  and  are  scattered  widely  over 
Marquette,  Waushara,  Green  Lake,  Columbia  and  Sank  counties,  pre- 
serving in  their  positions  a  sort  of  rough  parallelism  to  the  southern 


458  GEOLOGY  OF  CENTRAL  WISCONSIN. 

and  eastern  borders  of  the  main  Archaean  mass.  There  is  no  proof 
at  hand  that  the  rocks  of  these  patches  are  unconformably  super- 
posed npon  Laurentian  strata,  but  the  contrast  between  them  and  the 
Laurentian  gneisses  and  schists,  their  resemblance  to  Huronian  rocks 
elsewhere,  and  more  especially  the  parallelism  just  referred  to,  strong- 
ly suggest  the  possibility  of  their  forming  part  of  a  continuous  band 
of  Huronian,  of  which  the  Lake  Superior  and  Oconto  areas  are  other 
portions,  encircling  the  Laurentian  core,  after  the  manner  of  the  later 
and  undisturbed  Silurian  accumulations.  Regarding  the  Black  river 
ferruginous  schists,  and  the  associated  gneisses  as  Huronian,  a  continua- 
tion of  the  same  belt,  completing  the  circuit,  may  possibly  exist  in 
the  northwestward  trending  gneissic  and  hornblendic  beds  of  the  low- 
er Chippewa,1  the  arenaceous  and  conglomeratic  quartzite  of  the  hills 
in  T.  32,  R.  7  "W.,  near  the  Chippewa  river,2  and  the  quartzite  and 
associated  pipestone  of  Rice  Lake,  in  Barron  county.3  This  idea  of 
a  continuous  Huronian  belt  encircling  a  Laurentian  core  is  thrown 
out  as  a  suggestion  only,  a  generalization  towards  which  the  facts  in 
my  possession  at  this  writing  would  seem  to  point.  At  present  all 
that  we  can  affirm  with  any  degree  of  certainty  of  the  great  crystal- 
line rock  area  of  northern  Wisconsin  is  that  most  of  its  rocks  are 
Laurentian,  that  on  its  northern  a'nd  northeastern  edges  are  some  un- 
doubted Huronian  beds,  and  that  on  its  southern  and  southwestern 
borders  are  again  rocks  between  whose  Laurentian  and  Huronian  age 
there  remains  some  question,  although  they  quite  probably  are  to  be 
assigned  to  the  latter  period. 

From  its  northeastern  corner  the  Wisconsin  Archaean  nucleus,  in- 
cluding now  both  Huronian  and  Laurentian  rocks,  sends  a  long  pro- 
jection across  the  Upper  Peninsula  of  Michigan  to  the  shores  of  Lake 
Superior,  possibly  connecting,  beneath  the  lake,  with  the  great  Cana- 
dian Archaean  area.  Thus,  from  the  earliest  Paleozoic  times,  the  rock 
depositions  skirting  the  Archaean  of  Wisconsin  on  the  east,  south  and 
west,  must  have  gone  on  independently  of  those  on  its  northern  side. 
The  outcrops  of  the  undisturbed  and  unaltered  Silurian  formations, 
which  succeed  one  another  in  receding  concentric  bands  on  the  east- 
ern, southern  and  western  sides  of  the  Archaean  of  Wisconsin,  are  the 
direct  continuations  of  the  outcrop  bands  of  a  series  of  strata,  which, 
after  following  the  southern  side  of  the  Canadian  Archaean  westward 
through  New  York  and  Canada,  make  a  great  curve  to  the  northward 
across  the  peninsula  between  Lakes  Huron  and  Erie,  and  also  across 

1  E.  T.  Sweet,  manuscript  report  and  also  Transactions  Wis.  Acad.  Sci.,  Vol.  III. 

2  E.  T.  Sweet,  Loc.  cit. 

3 Owen's  Geological  Survey  of  Iowa,  Wisconsin  and  Minnesota. 


GENERAL  GEOLOGICAL  STRUCTURE.  459 

the  Upper  Peninsula  of  Michigan,  and  enter  "Wisconsin  on  its  north- 
eastern corner  with  a  sharp  southwestward  trend,  having  thus  accom- 
modated themselves  to  the  southern  line  of  the  ancient  Archaean  con- 
tinent. On  crossing  into  Wisconsin,  these  formations  dip  quite  rap- 
idly to  the  eastward,  and  their  southward  trending  outcrops  succeed 
one  another  in  comparatively  narrow  bands.  As  they  are  traced 
southward,  however,  these  outcrops  curve  gradually  westward,  the 
eastward  dip  at  the  same  time  lessening,  and  the  exposed  portion  of 
each  formation  becoming  wider.  Along  the  central  north  and  south 
axis  of  the  state,  the  eastward  dip  has  entirely  disappeared,  each  form- 
ation is  the  surface  rock  over  a  wide  extent  of  country,  and  the  bound- 
ing line  of  each  makes  a  wide  bow  to  the  southward  before  the  return 
northwestward,  parallel  to  the  western  side  of  the  Archaean  area. 
Thus  it  follows  that  in  the  Central  Wisconsin  district  are  to  be  ob- 
served a  smaller  number  of  the  Silurian  formations  than  occur  further 
eastward  and  westward  in  the  state. 

The  latest  one  of  the  Silurian  formations  of  Central  Wisconsin  is 
of  the  age  of  the  Trenton  limestone  of  New  York.  Elsewhere  in 
the  state,  the  Upper  Silurian  is  represented  by  immense  thicknesses  of 
limestone,  and  over  a  small  area  near  Milwaukee,  even  Devonian  beds 
are  to  be  seen.  The  exact  extent  to  which  the  original  areas  of  these 
various  formations  exceeded  their  present  ones,  it  is  quite  difficult  to 
arrive  at,  so  great  has  been  the  amount  of  denudation. 

After  the  close  of  the  Silurian  —  for  much  of  Central  Wisconsin 
probably  after  the  close  of  the  Lower  Silurian  —  no  farther  deposi- 
tions of  any  kind  were  made  until  the  time  of  the  Glacial  Drift, 
when  immense  masses  of  gravel  and  boulders,  as  also  stratified  sands 
and  clays,  were  largely  deposited.  During  all  of  the  intervening 
time  the  region  must  have  been  out  of  water  and  exposed  only  to  the 
ordinary  subaerial  eroding  agencies.  Thus  we  see  how  it  is  that  we 
find  here  proofs  of  a  denudation  unusually  great  for  non-monntainous 
regions. 

The  following  table  shows  at  a  glance  the  several  formations  that 
enter  into  the  structure  of  the  Central  Wisconsin  district,  with  their 
geological  relations: — 


460 
QUATERNARY. 


LOWER 

SILURIAN. 


AECH^AN. 


GEOLOGY  OF  CENTRAL  WISCONSIN. 

Recent  —  Peat  beds;  bog  iron  ores. 

Champlain  —  Lacustrine  clays,  over  200  feet  thick. 

Glacial  —  "  Drift";  including  bowlders,  till,  sand,  gravel,  etc. 

C  Galena  limestone;  dolomite,  300  to  350  feet. 
Trenton.        ~{    Trenton  limestone;   alternating  limestones  and 
[       dolomites;  in  all  100  to  120  feet. 

{St.  Peters  sandstone;  15  to  120  feet. 
Lower  Magnesian  limestone;   dolomite,   50  to 
125  feet. 

J    Madison  sandstone    beds,  35 
to  50  feet. 

Mendota  limestone   beds,  30 
to  45  feet. 

Including  possibly  two  dis- 
Primordial.  ~{  kinck  formations,  the  one 

lying  upon  the  eroded  sur- 
Lower  or  Pots-  j       face  of  the  other;  in  all  800 
dam  sandstone.  '        to  1000  feet  thick,  but  vary- 
ing much  on  account  of  the 
irregular  surface  of  the  un- 
derlying rocks. 

{Quartzites,  schists,  quartz-porphyries,  silicious 
iron  ores,  gneiss  (?);  many  thousand  feet 
thick. 

C  Gneiss,  granite,   schist,  diorite,  quartzite,  etc.; 
Laurentian.  <       no  crystalline  limestone;  many  thousand  feet 
thick. 


THE  ARCELEAN  ROCKS.  461 


CHAPTER  III. 
THE  ARCH^AN  ROCKS. 

THE  MAIN  ARCH^AN  AREA. 

I.  In  General. 

The  crystalline  rocks  of  the  Central  Wisconsin  district  may  be  con- 
veniently separated  into  two  groups,  for  the  purposes  of  description ; 
those  of  the  main  Archaean  body  constituting  one  of  these,  and  those 
which  occur  in  isolated  protruding  patches  within  the  region  of  the 
Silurian  sediments,  the  other.     The  two  are  of  course  but  parts  of  the 
same  grand  mass,  which  everywhere  underlies  the  undisturbed  Silu- 
rian beds,  a  fact  proven,  not  merely  by  geognostical  theory,  nor  the 
evident  passage  of  the  crystalline  rocks  beneath  the  Silurian,  but  also 
by  the  numerous  Artesian  borings  which  have  penetrated  through  the 
horizontal  strata  into  the  underlying  Archaean,  at  points  widely  scat- 
tered over  the  state.     At  present,  however,  we  have  to  do  only  with 
those  of  the  crystalline  rocks  that  appear  at  the  surface. 
The  area  occupied  by  the  rocks  of  the  main  Archaean  mass,  so  far  as  the 
district  at  present  under  consideration  is  concerned,  covers  all  of  Mara- 
thon, most  of  Wood,  and  much  of  Clark,  Jackson  and  Portage  counties. 
The  line  of  junction  between  the  Archaean  area  and  that  of  the 
next  formation  to  the  south,  the  Potsdam,  or  Lower,  sandstone,  is 
exceedingly  irregular,  and  often  quite  difficult  to  trace.     The  sand- 
stone is  frequently  found  stretching  far  northward  along  the  water- 
sheds between  the  southward  flowing  streams,  whilst  the  gneissic  and 
other  crystalline  rocks  are  to  be  observed  stretching  as  far  south  along 
the  stream  valleys,  the  areas  of  the  two  formations  thus  dovetailing 
into  one  another.     Thus  the  Wisconsin  and  the  Black  rivers  make 
rapids  over  tilted  gneissic  strata  for  many  miles  south  of  their  first 
entrance  upon  the  sandstone  region,  and  as  their  courses  are  followed 
downwards  the  exposures  of  these  rocks  are  to  be  found  more  and 
more  closely  restricted  to  the  stream  limits,  until  they  finally  occur 
in  the  river  beds  only,  the  sandstone  overlying  them  in  the  banks. 
A  more  definite  idea  of  the  position  of  the  boundary  line  between  the 
sandstone  and  Archaean  areas  may  be  obtained  from  the  general  geo- 
logical map  of  the  state  (Atlas  Plate  I),  and  also  from  Plate  XY  of 


462 


GEOLOGY  OF  CENTRAL  WISCONSIN 


FIG.  1. 


the  Atlas,  \vliich  give  the  boundary,  for  the  region  examined  by  the 
writer,  with  as  great  accuracy  as  present  knowledge  will  permit. 

The  imconformability  between  the  tilted  crystalline  rocks  and  the 
horizontal  sandstones  is  frequently  to  be  observed  along'the  boundary 
line  between  the  areas  of  the  two  formations,  and  especially  where 

the  streams  have  cut 
through  the  sand- 
stones into  the  un- 
derlying Archoean 

/=~l  "^lL__  ^sllr^J     In  a  number  of  places, 

f  jr.  4f=____^3>^^»^»-_-'--  S^=^__,___      *^7     as   to   which   details 

are  given  in  sub- 
sequent pages,  the 
sxact  junction  of  the 
two  formations  can 
be  seen.  In  one 
place  on  Black  river 
it  is  even  possible  to 
obtain  hand  speci- 
mens showing  both 
formations,  and  their 
respective  bedding 
and  lamination  lines. 


SKETCH  OF  A  SPECIMEN  FROM  NBAS  BLACK  RIVER  FALLS,  SHOW-      1*  ig.  1   IS  taken    Il'Oin. 

ING   THE    EXACT   JUNCTION   OF  THE    POTSDAM    SANDSTONE  AND  AR- 

.  ,«  .,       .  .    *   >  one 

CHJEAN  SCHISTS  ;  half  the  original  size. 


of        fllP^P 


specmens. 
The  general  topographical  features  of  the  crystalline  rock  dis- 

trict have  already  been  indicated.  It  is  an  elevated  area  with  an 
altitude  of  from  500  to  900  feet,  and  highest  on  the  north.  In  gen- 
eral, it  may  be  said  to  have  a  surface  of  gradual,  though  considerable, 
changes  in  elevation.  Looked  at  more  minutely,  however,  the  surface 
is  observed  to  be  broken  up  frequently  by  low  and  narrow,  but  quite 
steep,  ridges,  often  with  rock  exposures  at  top.  The  whole  region  is 
densely  timbered,  chiefly  by  pine.  These  pine  trees,  on  account  oi! 
the  small  depth  of  their  roots,  are  easily  and  frequently  prostrated  by 
the  wind,  often  over  many  square  miles  at  once.  Such  windfalls, 
when  burnt  over  and  grown  up  with  a  small  second  growth,  combine 
with  the  steep  rocky  ridges  and  the  numerous  small  intervening 
marshes,  to  render  traveling  in  this  region  to  the  last  degree  difficult. 
On  the  higher  swells  of  the  country,  however,  the  pine  is  often  re- 
placed by  hard  wood,  maple  especially.  In  such  parts,  traveling  is 
easier,  and  excellent  farms  are  obtained  by  clearing.  The  soil  in  these 


THE  ARCILEAN  ROCKS. 

cases  sometimes  evidently  results  for  the  most  part  from  a  direct  disin- 
tegration of  the  felspathic  rocks  in  place,  but  sometimes  also  from  a 
disintegration  of  similar  rocks  in  the  drift.  The  descent  of  the  re- 
gion southward  has  caused  the  river  valleys  and  smaller  watercourses 
to  be  cut  deeply  into  the  rocks,  which  are  hence  best  exposed  along 
streams.  As  already  said,  however,  exposures  occur  also  somewhat 
widely  scattered  away  from  the  streams.  Some  large  areas,  as,  for 
instance,  the  country  along  the  Fourth  Principal  Meridian,  from 
town  30  to  town  42,  are  without  rock  exposures,  the  drift  covering 
being  especially  heavy. 

By  far  the  most  common  one  of  the  crystalline  rocks  in  this  area 
is  gneiss ;  next  in  order  of  abundance  are  granitoid  gneiss,  granite, 
syenite,  hornblende  rocks,  chloritic  schists,  mica-schists,  quartz-schists, 
quartzite  and  felsitic  rocks.  In  one  small  district  on  Black  river  in 
Jackson  county  are  large  exposures  of  silico-ferruginous  schists  (iron 
ores),  associated  with  silico-magnesian  (talcose)  schists.  All  of  these 
general  kinds  include  many  varieties,  which  are  noted  in  the  follow- 
ing detailed  descriptions.  The  granitoid  and  gneissoid  kinds  have 
most  commonly  a  moderately  coarse  character. 

The  original  bedded  condition  of  the  whole  series  is  rendered  suf- 
ficiently evident,  not  only  by  a  prevailing  gneissoid  and  schistose 
character,  but  also  by  the  existence  of  distinct  bedding  planes 
and  lamination  lines,  which,  though  often  obscured  by  cross-jointing, 
especially  in  the  granitoid  kinds,  can  nevertheless,  in  general,  be 
readily  made  out.  Th#t  the  processes  of  metamorphism  and  disturb- 
ance have  been  carried  almost  to  their  last  extremes  is  shown  by  the 
highly  crystalline  character  of  the  rocks,  the  grading  of  the  gneiss 
into  granite,  the  greatly  contorted  condition  of  the  gneiss  laminae,1 
atid  the  close  folding  of  the  whole  series.  In  some  places,  portions 
of  the  arches  are  left;  but  in  general  erosion  has  removed  or  ob- 
scured all  the  crowns,  and  has  made  of  what  must  once  have  been  a 
lofty  mountainous  region,  one  in  which  the  variations  from  a  general 
level  are  only  those  of  insignificant  ridges,  and  comparatively  shallow, 
eroded  watercourses. 

Whilst  the  bedding  of  the  whole  series  is  thus  evident,  distinctly 
intrusive  granite  occurs,  its  nature  being  indicated  by  the  way  in 
which  it  joins  and  penetrates  the  bedded  rocks.  This  extravasated 
granite  is  usually  of  a  pinkish  to  reddish  color,  often  very  bright 
red,  and  occurs  in  very  large  masses. 

A  tendency  to  weather  characterizes  most  of  the  gneisses  and  other 

1  Most  beautifully  exhibited  on  Black  river,  just  below  the  crossing  of  the  Green  Bay 
Railroad. 


464  GEOLOGY  OF  CENTRAL  WISCONSIN. 

felspathic  rocks,  and  also  those  that  are  largely  hornblendic.  The  alter- 
ation usually  extends  but  a  small  distance  into  the  body  of  the  rock, 
which  can  generally  be  observed  in  its  true  unaltered  character  by  re- 
moving the  surface  crust.  In  some  localities,  however —  and  these  are 
altogether  without  the  drift  area,  or  at  least  where  the  drift  materials 
are  scanty  —  the  whole  exposed  portion  of  the  rock  is  so  disintegrated 
as  to  crumble  to  dust  under  a  blow  of  the  hammer,  or  is  completely  al- 
tered, by  removal  of  alkaline  ingredients  and  absorption  of  water,  to  a 
clayey  mass,  which,  when  the  original  rock  was  non-ferruginous,  or 
when  the  iron  oxides  have  been  also  completely  removed,  is  a  mixture 
of  pure  kaolinite  and  quartz  grains,  and  is  of  considerable  commercial 
value.  The  almost  entire  restriction,  so  far  as  known,  of  this  kaolin- 
ized  rock  to  those  districts  where  there  is  nothing  to  indicate  the 
former  presence  of  the  glacial  agencies,  is  a  fact  of  very  considerable 
interest.  Its  absence  everywhere  where  the  drift  occurs  may  indicate 
that  it  has  been  removed  by  the  drift  forces.  It  is  true,  however, 
that  the  kaolin  district  coincides  with  one  in  which  there  is  generally 
more  or  less  of  a  sandstone  covering  to  the  crystalline  rocks,  and  that 
many  of  the  kaolin  occurrences  are  beneath  a  few  layers  at  least  of 
sandstone.  It  may  then  be  that  the  surface  waters,  percolating 
through  the  porous  sandstone  —  in  ancient  times  much  thicker  than 
now  —  have  formed  natural  watercourses  along  the  junction  between 
it  and  the  less  easily  penetrable  crystalline  rocks,  and  have  thus  ex- 
erted an  unusual  disintegrating  action;  whilst  the  sandstone  itself 
has  subsequently  acted  as  a  preserver  of  the  kaolinized  rock  from  the 
ordinary  eroding  agencies. 

No  one  system  of  strikes  prevails  over  the  whole  region,  but  yet 
for  long  distances  a  marked  parallelism  can  be  observed  in  the  courses 
of  the  outcrops  of  the  various  layers.  Thus  along  the  Wisconsin 
from  its  southernmost  exposures  of  crystalline  rocks,  at  Point  Bass, 
in  Wood  county,  as  far  north  as  Wausau,  in  Marathon  county,  the 
strikes  are,  for  the  most  part,  east  of  north,  whilst  the  dips,  though 
of  course  far  less  constant  in  amount  and  direction,  are  more  com- 
monly north  than  south.  On  Black  river,  again,  for  the  whole  dis- 
tance examined,  the  strikes  are  just  as  markedly  northwest,  and  on 
Yellow  river  more  commonly  west,  than  east  of  north.  Whilst  no 
general  system  of  strikes  can  be  laid  down  for  the  whole  region,  and 
no  further  generalizations  can  be  drawn  from  the  observations  made 
in  the  Central  Wisconsin  district,  it  is  nevertheless  very  probable  that 
by  comparing  the  results  of  different  observers  on  the  strike  direc- 
tions for  the  whole  Archrean  region  of  the  state,  some  quite  import- 
ant conclusions  may  yet  be  reached.  At  the  time  of  writing  investiga- 


THE  ARCILEAN  EOCKS.  465 

tions  on  this  region  are  still  in  progress,  and  such  generalizations 
would  now  be  premature.  Attention  may  be  drawn,  however,  to  the 
fact  that  the  general  directions  of  the  strikes  preserve  a  sort  of  paral- 
lelism to  the  sides  of  the  somewhat  irregularly  shaped  Archaean  area. 
Thus,  on  the  Wisconsin,  Wolf,1  Peshtigo2  and  Oconto,8  the  strikes 
are  northeastward,  coinciding  with  the  long  boundary  line  on  the 
southeast  side;  on  the  Black,  Yellow,  and  lower  Chippewa,  the  di- 
rections are  northwestward,  corresponding  in  general  to  the  south- 
western boundary  line;  on  the  upper  Chippewa,  and  in  the  Penokee 
region,  the  strikes  are  generally  north  of  east,  corresponding  with  the 
Lake  Superior  side  of  the  Archaean  area.  Whether  this  correspond- 
ence has  any  significance  or  not,  remains  to  be  seen.  It  is  quite  pos- 
sible that  the  northwestward  strikes  of  the  Black,  Yellow  and  lower 
Chippewa  indicate  the  existence  of  a  continuous  band  of  Huronian 
(including  then  gneissic  rocks  and  granites)  which,  curving  around  to 
the  north  and  northeast,  includes  the  quartzites  of  Rice  lake,  in  Bar- 
ron  county,  and  joins  finally  with  the  Iron  Range  series  of  Ashland 
county.  The  remaining  northeastward  strikes,  on  this  view,  would 
be  those  of  the  original  Laurentian  nucleus. 

It  has  already  been  said  that  most  of  the  rocks  of  the  main  Archaean 
area  are  referred  to  the  Laurentian.  This  is  done  partly  because  of 
their  general  lithological  characters,  but  more  especially  because 
they  are  found  near  Lake  Superior,  and  also  near  the  Michigan  bound- 
ary, in  Oconto  county,  underlying  unconformably  other  metamorphic 
beds,  chiefly  of  a  slaty  character,  which,  from  their  relations  both  to 
the  Copper-bearing  series  and  Silurian  sandstones  of  Lake  Superior, 
and  to  the  Potsdam  sandstone  of  Central  Wisconsin,  quite  evidently 
occupy  the  horizon  of  the  Canadian  Huronian.  When  these  relations 
are  taken  into  account  with  their  great  resemblance  in  lithological 
characters  to  the  typical  Canadian  formations,  from  which  they  are 
but  little  removed,  and  with  which  they  are  indeed  quite  probably 
continuous  underneath  the  waters  of  Lake  Superior,  the  reference  of 
the  two  Wisconsin  series  of  crystalline  rocks  to  the  Laurentian  and 
Huronian  seems  unavoidable. 

The  undoubted  Huronian  beds  of  Wisconsin  lie  entirely  without 
the  district  which  is  the  object  of  the  present  report.  Those  lying 
within  the  district,  on  Black  and  Yellow  rivers,  already  alluded  to  as 
doubtfully  Huronian,  are  as  yet  too  doubtfully  so  to  merit  further  at- 
tention in  this  place. 

The  only  materials  of  economic  importance  yet  known  to  occur 
in  the  Archrean  of  Central  Wisconsin  are  kaolin  or  rotted  rock,  and 

1  Manuscript  report,  E.  T.  Sweet.        *  Oral  communication,  T.  C.  Chamberlin, 
Wis.  SUB.— 30 


466 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


building  stones,  especially  ornamental  building  granite.  Beds  large- 
ly charged  with  the  specular  and  magnetic  oxides  of  iron  occur  on 
Black  river,  but,  so  far  as  known,  contain  too  little  iron  to  be  used  as 
ores  of  that  metal.  Judging  from  the  character  of  the  rocks  of  this 
age  in  Canada,  a  great  variety  of  materials  of  economic  importance 
might  reasonably  be  expected,  including  the  precious  metals,  lead, 
copper  and  iron  ores,  all  of  which  are  found  and  profitably  worked  in 
the  Canadian  Archaean.  Small  traces  of  precious  metals  have  been 
found  in  quartz  from  Clark  county.  Details  as  to  the  kaolins  of  the 
Black,  Yellow  and  Wisconsin  rivers,  and  as  to  the  ornamental  granites 
of  Yellow  river  and  other  places,  are  given  on  subsequent  pages. 
Both  of  these  materials  are  obtainable  in  large  quantity,  and  are  des- 
tined to  become  important  factors  in  the  industries  of  the  state.  The 
red  granites  are  quite  extraordinary  in  their  fine  qualities,  and  are 
hardly  to  be  equaled  by  any  in  the  country. 

II.    Local  Details. 

The  various  rock  exposures  belonging  to  the  main  Archaean  area 
which  have  been  examined  by  the  writer,  are  chiefly  in  the  vicinities 
of  the  three  main  streams,  the  Wisconsin,  Yellow  and  Black,  and 
their  tributaries.  A  corresponding  grouping  of  the  detailed  descrip- 
tions is  here  adopted,  the  valley  of  each  stream  being  followed  up 
wards  from  its  southernmost  crystalline-rock  exposure. 

UPPER   WISCONSIN   VALLEY. 


FIG.  2. 


At  Whitney's  "Rapids,  near  Point  Bass,  on  the  S.  W.  qr.  of  Sec.  10,  and  the  N.  W. 
qr.  of  Sec.  15,  T.  21,  R.  5  E.,  occur  the  southernmost  exposures 
of  crystalline  rocks  on  the  Wisconsin  river.  They  are  here  con- 
fined entirely  to  the  river  bed,  the  horizontal  Potsdam  sandstone 
overlying  them  in  the  banks.  The  following  sketch  map  serves 
to  show  the  occurrence  of  the  various  outcrops  at  this  point. 

The  southernmost  exposure  seen,  and  this  only  at  unusually  low 
stages  of  the  water,  is  a  low  rounded  one  of  quartzose  gneiss  (869), 
a  few  square  yards  in  area,  in  the  river  bed  at  the  point  E  of  the 
map.  Ten  paces  up  the  stream  from  here  is  a  similar  exposure 
of  a  greenish-black,  pyritiferous,  hornblendic  rock  (870),  traversed 
by  pinkish  felspathic  veins,  and  striking  N.  50°  E.^with  a  nearly 
vertical  dip.  Continuing  northward  along  the  bed  of  the  stream, 
between  the  western  shore  and  the  island  I),  we  find  occasional 
exposures  of  decomposing  gneiss,  which  is,  for  the  most  part, 
v  jmm  concealed  by  water  and  river  gravel.  At  about  eighty  paces,  a 

i  i   wfm       secti°n  across  the  stream  was  taken,  on  the  line  C  D  of  the  map, 

— ' '  which  is  represented  by  Fig.  3.     Here  the  white,  kaolinized,  bill, 

VICINITY  OF  POINT  BASS,    ,••>•,  £  •    •          i      /OI-M\  1-11  /*    • 

still  firm,  gneissic  rocks  (871)  are  overlaid  by  2  to  6  inches  of 
V>  OOD  COUNTY. 

sandstone,  the  lowest  layer  of  which,  about  2  inches  thick,  in 
Scale,  1  mile  to  the  inch.    ,  .   ,  ,       ,  ,       ...  ..         ....        . 

highly  charged  with  pyrite,  which,  ui  places,  excludes  the  sand 
1  All  bearings  are  referred  to  the  true  meridinn. 


THE  ARCILEAN  ROCKS. 


467 


entirely.  The  upper  sand- 
stone layers  are  coarse  and 
brownish-colored,  and  lie  in 
large,  flat  slabs,  giving  the 
river  bed,  for  many  rods, 
the  appearance  of  a  paved 
street. 

On  the  line  A  B  of  the 
map,  a  section  was  meas- 
ured across  the  stream, 
which  is  shown  in  Fig.  4. 
At  the  southeast  end  of  this 
section  a  vertical  cliff  of 
heavily  bedded  sandstone, 
35  feet  high,  forms  most 
of  the  river  bank.  Be- 
neath the  sandstone, 
gneiss  shows  for  about  5 
feet  down  to  the  water's 
edge.  Its  upper  portions 
are  altered  to  a  soft  kaolin, 
about  2  feet  in  thickness. 
Immediately  at  the  foot  of 
the  cliff  runs  the  main 
channel  of  the  river,  here 
about  400  feet  in  width. 
Beyond  it  to  the  northwest, 
a  series  of  low  outcrops  of 
gneiss  alternate  with  nar- 
row water  channels  across 
the  remainder  of  the  river 
bed.  The  first  exposure 
beyond  the  main  channel 
was  not  reached.  The  next 
showed  a  coarse  -  grained, 
pink-  white-and-black-mot- 
tled,  quartzose,  gneissoid 
granite  (864),  striking  N.  42°  E.,  and  dipping  north- 
westward 70°,  with  marked  bedding  planes.  A  second 
set  of  joints,  much  less  marked,  strikes  N.  50°  W., 
and  dips  80°  N.  E.  The  quartz  of  this  rock  is  hyaline, 
and  in  fine  grains  aggregated  into  large  blotches;  the 
mica  is  blackish  and  fine-grained,  and  aggregated  along 
certain  lines;  and  the  felspar  is  both  white  and  pink,  in 
large  facets.  The  weathered  surface  is  brownish  and  dull, 
with  a  white  undercrust,  and  deeply  pitted  from  kaoliniza- 
Uon  of  the  felspar.  Quartz  veins,  a  few  inches  in  width, 
traverse  the  exposure  in  an  east  and  west  direction,  stand- 
ing vertically. 

The  next  exposure  to  the  northwest  on  the  line  of  the 
section  is  71  feet  wide  and  of  the  same  rock  (865)  as  the 
last,  with  rather  more  felspar,  and  showing  the  same 


*  *§• 


s.S" 


*  * 


468  GEOLOGY  OF  CENTRAL  WISCONSIN. 

bedding.  A  red  felspathic  vein  was  noted,  2  inches  wide,  dipping  70°  N.,  and  also  the 
same  east  and  west  quartz  veins  as  before.  Towards  the  northwest  end  of  this  ex- 
posure the  gneiss  is  quite  thoroughly  decomposed  into  a  crumbling,  earthy- textured, 
brown-  and  white-blotched  material,  showing  still  a  few  mica  flakes  and  quartz  granules 
in  the  interior,  and  containing  4.96  per  cent,  of  water.  The  same  partly  kaolinized 
rock  is  found  all  along  the  section  until  the  west  bank  of  the  river  is  reached,  showing, 
however,  still  quite  plainly  the  lamination  and  bedding  planes  of  the  unaltered  rock,  the 
dip  and  strike  remaining  the  same.  At  the  foot  of  the  west  bank,  which  is  about  20 
feet  in  height,  unaltered  quartzose  granite  shows,  with  north  and  south  quartz  veins  % 
inch  thick.  Above  this,  and  some  few  feet  above  the  water  level,  fine,  white,  soft  kaolin 
shows  in  a  little  swamp,  and  above  this  again  are  seen  a  few  thin  layers  of  the  sand- 
stone. 

On  the  N.  W.  qr.  Sec.  10  are  openings  in  the  river  bank,  here  some  20  feet  in  height, 
showing  a  considerable  quantity  of  white  kaolin.  The  various  exposures  are  at  differ- 
ent levels,  and  may  indicate  a  thickness  of  as  much  as  15  feet  in  some  places,  but  as  the 
clay  is  merely  an  alteration  of  the  gneissic  rock  in  place,  it  forms  no  continuous  bed, 
the  less  altered  portions  of  the  rock  occasionally  rising  entirely  through  it.  At  the 
principal  opening  22  inches  of  soft,  bluish-white  clay  were  noticed.  The  following  are 
analyses  of  samples  from  this  place: 

861.  862. 


Potash  

A. 

1  .  25 

s 

2.81 

Soda  

08 

trace 

Iron  

2.88 

Water  

A  B 

1.51  1.54 
.81  .22 

1.17 


861  A  is  the  raw  kaolin  from  the  lower  part  of  the  exposure;  861  B  is  the  fine  or  ka- 
olinite  portion  of  861  A,  separated  by  levigation.  Nos.  862  A  and  862  B  are,  in  like 
manner,  raw  and  washed  clay  from  the  upper  part  of  the  same  opening.  The  amounts 
of  alkalies  are  considerable,  and  no  lessening  in  their  percentages  appears  to  be  effected 
by  levigation.  The  state  of  oxidation  of  the  iron  was  not  determined,  but  it  would  ap- 
pear to  be  chiefly  in  the  protoxide  state,  judging  from  the  color  of  the  clay.  These  facts 
would  indicate  a  less  thorough  kaolinization  here  than  at  other  places  in  the  vicinity. 
Immediately  above  the  kaolin  openings  are  two  feet  of  coarse,  brownish,  friable  sand- 
stone, whilst  below  it,  down  to  the  water's  edge,  gneiss  in  decreasing  stages  of  decom- 
position is  seen.  At  the  foot  of  the  bank  is  a  low  exposure  of  unaltered,  fine-grained, 
light-colored  gneissoid  granite  (868).  The  three  ingredients  of  the  rock  are  all  distinctly 
visible,  the  felspar  being  both  pink  and  white,  the  latter  without  apparent  striations; 
the  quartz  is  abundant,  in  hyaline  grains;  the  mica  is  aggregated  into  layers  and  pro- 
duces a  greasy  feeling  on  some  surfaces  of  lamination. 

At  the  foot  of  the  rapids,  on  the  west  side  of  the  Wisconsin,  just  above  Port  Edward, 
on  Sec.  25,  T.  22,  R.  5  E.,  a  rather  coarse  grained,  mottled,  red-weathering  gneissoid 
granite  (879)  is  exposed.  A  distinct  parallel  grain  is  perceptible,  with  corresponding 
bedding  joints,  which  strike  N.  45°  E.  and  dip  50°  N.  W.  Other  joints,  which  make 
large  smooth  faces,  strike  N.  75°  E.  About  50  feet  further  up  stream  is  exposed  a  coarse- 
grained, pinkish,  highly  felspathic  rock,  which  shows  a  very  distinct,  sometimes  con- 
torted, lamination,  trending  in  the  same  N.  45°  E.  direction  as  before.  In  this  rock 
the  mica  is  nearly  excluded  by  the  felspar  and  quartz,  which  themselves  are  largely 
separated  into  distinct  bands.  In  places  much  pyrite  is  present.  Fifty  feet  further  a 
low  exposure  shows  an  apparent  JN .  50°  W .  strike,  but  this  seems  to  be  due  to  numer- 
ous close  veins  running  in  this  direction,  for  a  few  feet  beyond,  the  same  strike  direc- 
tion as  before  observed  reappears,  accompanied  now  by  a  southeast  dip,  in  a  fine 


THE  ARCfiffiAN  ROCKS.  469 

grained,  greenish,  decomposing,  pyritiferous,  mica-schist  (881).  At  the  fall  at  the  up- 
per end  of  the  channel  the  rock  is  hard,  very  fine-grained,  light-colored,  distinctly,  banded 
gneiss  (882),  containing  much  quartz  and  greenish,  greasy  mica  along  the  lamination 
planes.  The  northeast  strike  and  southeast  dip  (50°)  show  here  very  plainly. 

It  would  appear  that  we  have  in  these  exposures  the  synclinal  line  at  which  the  north- 
west clip  of  all  the  beds  further  down  the  river  gives  place  to  the  southeast  one  which 
prevails  for  many  miles  above. 

Continuing  now  along  the  west  bank  of  the  Wisconsin,  we  note  next  an  occurrence 
of  kaolin  on  the  land  of  Mr.  L.  P.  Powers,  lot  5,  sec.  24,  T.  22,  R.  5  E.  The  kaolin 
is  exposed  naturally  in  the  river  bank  at  several  points,  and  has  been  at  one  place  laid 
bare  by  digging,1  several  carloads  having  been  sent  away  for  trial.  The  exposures  are 
some  ten  feet  above  the  river  at  low  water,  and  show  an  apparent  thickness  of  about 
three  feet.  Much  of  this  is  pure  white,  plastic  clay,  easily  removed  with  a  spade,  but 
in  many  places,  and  especially  towards  the  base  of  the  exposure,  it  grades  into  a  par- 
tially altered  rock  of  varying  degrees  of  firmness.  In  much  even  of  the  perfectly  soft 
clay  the  lamination  planes  of  the  unaltered  rock  are  still  distinctly  to  be  seen,  and  thin 
plates  of  solid  quartz  remain  in  their  original  positions,  dipping  east  of  south,  at  about 
65°.  Where  these  lines  are  so  distinct  the  clay  is  frequently  of  a  bluish  cast,  and  then 
appears  to  be  less  refractory  than  usual.  All  of  it  tends  to  be  stained  superficially  by  a 
brownish  oxide  of  iron,  which  may  be  due  to  the  infiltration  of  ferruginous  waters,  and 
is  not  in  sufficient  quantity  to  affect  the  value  of  the  clay.  In  a  few  places,  however, 
large  dark-reddish  patches  are  seen  imbedded  in  the  white  clay,  and  are  undoubtedly 
due  to  the  presence  of  a  large  and  pernicious  quantity  of  iron  oxide.  Immediately 
above  the  kaolin  is  found  a  layer,  1%  feet  thick,  of  quartz  fragments,  mostly  angular, 
and  evidently  derived  from  the  decomposing  rock  just  below.  Above  this  in  a  few 
places  are  to  be  seen  one  or  two  thin  layers  of  crumbly,  brownish  sandstone,  a  remnant 
of  the  sandstone  which  overlies  the  crystalline  rocks  everywhere  in  the  vicinity.  Above, 
again,  is  found  the  soil,  three  feet  in  thickness.  Below  the  kaolin,  at  the  water's  edge, 
low  exposures  of  unaltered  gneiss  appear.  A  series  of  specimens  for  analysis  obtained 
from  this  place  yielded  the  following  results :  — 

822  823  S24  825 


Silica   

A             B                  AS 

..     70.82    
18  98     

A             B 

70.25     .... 
17.68     

69.34 
19.19 

Iron  peroxide  .  .  . 

..       1.24    .....          2.34    
.24    

2.32     .... 
.33     

1.75 
.44 

.02     

1.49     .... 

.39 

Potash 

2  49      1.21         2.30      1.96 

1.69    2.33 

3.30 

goda      

.10     trace         trace     trace 

.39      .10 

2.43 

~\V"atcr    

..      5.45      8.84        6.30 

5.61    8.84 

2.67 

02    

99.36     

99.76     

99.51 

Specific  gravity  . 

..      2.55     

2.50     .... 

2.85 

822  A  is  from  the  exposure  furthest  down  stream,  and  was  analyzed  just  as  taken 
from  the  ground,  after  drying  at  100°.  It  represents  a  thickness  of  about  three  feet. 
It  will  be  noticed  that  the  alkali  is  chiefly  potash,  a  fact  winch  seems  to  be  attributable 
to  the  greater  difficulty  with  which  the  potash  felspar  decomposes,  both,  potash  and  soda 
felspars  entering  into  the  composition  of  the  gneisses  of  the  vicinity.  The  small  trace 

1  This  iiaolin  has  been  much  farther  developed  since  the  time  of  my  examination  in  1874. 


470 


GEOLOGY  OF  EASTERN  WISCONSIN. 


Fig.  5. 


of  carbonic  acid  remains  as  an  indicator  of  the  mode  of  decomposition  which  has  led  to 
the  formation  of  the  kaolin.  822  B  is  the  fine  portion  of  the  same  clay  separated  by 
levigation  in  the  laboratory  from  the  admixture  of  coarse  sand  composed  of  quartz  and 
undecomposed  felspar  fragments,  the  former  predominating.  The  smaller  percentage 
of  alkalies  is  due  to  the  removal  of  the  felspar  fragments  and  mica  flakes.  823  A  and 
823  B  are  raw  and  washed  clay  from  the  next  exposure  above,  along  the  stream.  A  les- 
sening of  the  alkali  percentage  is  again  to  be  observed  in  the  washed  clay.  823  repre- 
sents an  apparent  thickness  of  nearly  three  feet.  824  is  from  the  exposure  furthest  up 
stream.  It  is  quite  soft  and  clayey,  but  in  places  retains  the  rock  lamination  to  a 
marked  degree.  824  A  and  824  B  are  respectively  the  raw  and  levigated  clay.  It  will 
be  noticed,  that,  although  retaining  the  rock  structure,  this  clay  is  yet  pretty  completely 
decomposed,  the  only  point  indicating  a  lack  of  thorough  decomposition  being  the  larger 
amount  than  usual  of  soda.  825  is  a  still  firm,  partly  decomposed  rock  from  the  same 
place  as  824.  It  is  of  a  dirty  white  color  on  the  exterior,  nearly  pure  white  on  the  inte- 
rior, quite  porous,  has  an  evident  gneissoid  texture,  and  is  speckled  with  small  flakes  of 
silvery  mica.  With  the  exception  of  this  mica  no  distinct  constituent  minerals  can  be 
seen  with  the  naked  eye;  with  a  magnifying  glass,  however,  a  fresh  fracture  reveals  in 
a  few  places  minute  grains  of  quartz  and  undecomposed  orthoclase  felspar.  The  large 
tenure  of  alkalies,  especially  of  soda,  and  the  small  amount  of  water,  indicate  the  only 
partial  decomposition. 

Appearances  would  indicate  the  existence  of  a  considerable  body  of  kaolin  at  this 
point.  Since  my  examination  the  locality  has  been  much  further  developed  and  a  large 
number  of  fire  brick  made.  In  1875,  Mr.  E.  T.  Sweet,  of  the  Geological  Survey,  vis- 
ited the  place  and  found  that  no  care  was  taken  to  select  the  clay,  nor  was  it  put 

through  any  washing  process  to  separate  the  unde- 
composed portions.  He  was  informed  that  woodash 
was  used  largely  to  counteract  the  shrinking  of  the 
clay  on  burning;  an  addition,  which,  of  course,  in- 
troduced the  ingredient  most  to  be  dreaded.  As  a 
result  of  this  method  of  manufacture  and  lack  of  se- 
lection, a  very  great  variation  was  observable  in  the 
quality  of  the  bricks,  some  even  showing  a  tendency 
to  agglomerate  in  the  kiln.  The  clay  from  this  local- 
ity has  also  been  largely  shipped  raw  to  Milwaukee 
where  it  has  been  used  by  the  Iron  Companies  and 
Gas  Light  Company.  In  1874,  about  one  thousand 
brick  were  burned  for  the  Gas  Light  Company  from  a 
mixture  of  the  Grand  Rapids  kaolin  and  pulverized 
fire-brick,  and  were  found  to  be  of  the  very  best  qual- 
ity.1 A  brick  made  in  this  way,  and  procured  for  me 
by  Mr.  S.  G.  Lapham,  yielded  2.06  of  potash  and 
0.31  of  soda.  It  presented  a  peculiar  jagged,  porous 
appearance  on  a  fracture,  with  blotches  of  a  white 
porcelain -like  substance,  and  was  said  to  be  an  excel- 
lent brick.  At  the  Bayview  Iron  Works2  the  clay 
has  been  tried  raw,  and  found  very  refractory. 

Bricks  made  from  it  and  used  here  were  found  to  vary  very  much  in  their  refractoriness, 
some  being  extraordinarily  refractory,  others  succumbing  readily  to  the  heat. 

On  Mr.  H.  Canning's  land  on  the  west  half  of  the  N.  E.  qr.  of  Sec.  26,  T.  22,  R.  5 
E.,  several  pits  and  a  well  have  been  sunk  into  decomposing  rock  and  kaolin.     Speci- 
mens from  here  yielded  the  following  analytical  results : 
»  Letter  from  Dr.  I.  A.  Lapham,  Milwaukee,  Nov.  13, 1874.      "  Letter  from  Mr.  J.  J.  Hagerman. 


VICINITY  OF  GRAND  RAPIDS, 

WOOD  COUNTY. 
Scale,  one  mile  to  the  inch. 


THE  AJRCH^EAN  ROCKS. 


471 


827 


838 


Silica 

Alumina 

Oxide  of  iron 1 . 93     .... 

Lime 

Magnesia 

Potash 1.84    2.65 

Soda 27       .21 

Water  .  ....     7.96 


2.95 
.83 


Fine  clay 

Coarse  residue. 


54.86 

28.87 

2.48 

.16 

.98 

2.57 

.07 

9.98 

99.97 

56.61 
43.39 

100.00 


826  A  and  826  B  are  the  raw  and  washed  kaolin  from  Mr.    Canning's  well;  827  is 
washed  clay  from  the  two  pits  on  the  same  land,  several  hundred  feet  from  the  well; 

828  is  the  fine  clay  levigated  from  an  ex- 
ceedingly white  unbaked  brick,  said  to  have 
been  made  from  clay  from  Mr.  Canning's 
well. 

The  next  rock  and  kaolin  occurrences 
that  we  note  in  ascending  the  Wisconsin 
are  those  in  the  vicinity  of  the  cities  of 
Grand  Rapids  and  Centralia.  The  localities 
are  shown  on  the  sketch  map,  Fig.  5. 

Here  the  river  makes  a  long  series  of  wild 
rapids  over  gneissic  rocks,  which  on  the 
shores,  at  short  distances  from  the  water, 
appear  at  several  points  altered  to  kaolin 
and  overlaid  by  a  few  thin  layers  of  sand- 
stone. 

One  of  the  most  instructive  occurrences  in 
the  vicinity  is  to  be  seen  on  the  roadside  in 
°  J>  the  city  of  Grand  Rapids,  near  the  Rablin 
House  (Point  A  on  Fig.  5).  Here  some  cut- 
ting has  been  done  into  the  bank  for  grad- 
ing the  street,  and  kaolin,  decomposing 
rock,  and  overlying  sandstone  laid  bare. 
The  following  is  the  section  obtained  here 
(Fig.  6.) 

A  specimen  of  decomposing  gneiss  (816), 
occurring  beneath  the  sandstone,  yielded : 

Potash 7.16 

Soda 5.02 

Water 3.55 

The  very  partial  nature  of  the  decompo- 
sition is  thus  rendered  evident.  In  appear- 
ance however,  nearly  all  resemblance  to  the 
original  rock  has  been  lost,  the  color  being 


•<  02 

M 


472  GEOLOGY    OF   CENTRAL  WISCONSIN. 

a  dirty  white,  and  the  interior,  though  still  firm  and  hard,  of  a  somewhat  earthy  tex- 
ture. In  some  fragments  a  few  minute  grains  of  unaltered  felspar  can  be  detected 
with  the  magnifier. 

From  the  gneiss  exposures  shown  at  thevwuter's  edge  in  the  sketch  just  given  (Fig.  6), 
the  following  measured  section  was  taken  entirely  across  the  great  ledges  of  gneiss 
which  form  the  Grand  Rapids  of  the  Wisconsin.  This  section  runs  N.  20°  W.,  on  the 
line  A  B,  or  at  right  angles  to  the  general  trend  of  the  layers,  which  is  usually  quite 
plainly  to  be  seen.  The  exposures  are  not  entirely  continuous  along  the  line  of  section, 
but  are  nearly  so,  and  gaps  could  be  filled  with  ledges  a  little  distance  on  one  side  or  the 
other.  At  the  time  of  our  examination,  the  river  was  low,  and  an. unusual  amount  of 
rock  laid  bare.  The  measurements  given  indicate  horizontal  widths.  Since  the  general 
dip  is  southeastward  the  first  beds  of  the  section  are  the  highest  in  the  series. 

Feet 

1.  Gneiss:  at  the  beginning  of  the  measurement  (833)  coarse-grained,  distinctly 

laminated,  black -white-and-pink-mottled;  striking  N.  80°  E.,  dipping  60° 
S.  E.  The  mica  of  this  rock  is  greenish  and  brownish,  and  aggregated 
into  large  blotches;  the  felspar  is  both  pink  and  white,  the  latter  not  plainly 
striated,  and  occurring  in  large  facets;  the  quartz  is  abundant  and  limpid. 
Pyrite  is  present  in  small  quantity.  Twenty-five  feet  from  the  beginning, 
the  felspar  is  much  increased  in  quantity  (834).  At  fifty  feet  the  grain  of 
the  rock  becomes  much  finer,  and  the  mica  is  largely  restricted  to  the  sur- 
faces of  the  quite  distinct  laminae  (835).  This  variety  gives  place  soon 
again  to  a  coarser  kind  (836),  similar  to  that  at  the  beginning  of  the  section 
(833),  but  with  the  quartz  somewhat  more  prominent.  At  seventy  feet  the 
bedding  directions  are  quite  plain  and  show  a  strike  of  N.  75°  E,  and  a  dip 
of  60°  S.  E.  Here  the  rock  laminse  are  contorted,  and  the  mica  very 
abundant,  almost  excluding  the  felspar.  A  few  pinkish  granite  veins  occur, 
from  ^  inch  to  2  inches  wide,  conforming  to  the  bedding  of  the  rock.  The 
vein  matter  (838)  is  predominatingly  of  pinkish,  flaky  quartz,  felspar  being 
subordinate,  and  the  mica  restricted  to  the  sides  of  the  vein, 100 

2.  Covered,  by  water,   20 

3.  Gneiss :  at  the  beginning  of  the  measurement  coarse-grained,  schistose,  con- 

torted in  places,  pinkish-white,  very  quartzose,  carrying  pyrite  (839),  strik- 
ing N.  85°  E.  Twenty  feet  beyond,  this  changes  to  a  finer-grained,  dark- 
grayish,  schistose  kind  (840),  embracing  some  thin  veins  of  white  quartz 
and  pinkish  granite.  At  30  feet,  the  strike  is  N.  80°  E.,  the  dip  65°  S.  E. 
At  80  feet  occurs  a  reddish  granite  vein  six  feet  wide.  The  vein-matter 
(843)  shows  a  fine-grained  texture  and  dark  reddish  color,  and  appears  to  be 
a  mixture  of  very  fine,  pinkish  felspar  facets,  and  translucent  quartz  grains, 
no  rnica  being  apparent.  At  100  feet  the  grain  becomes  coarser  again  until 
at  130  feet  (844),  the  rock  is  again  like  that  at  the  beginning  of  the  section 
(833).  Beyond,  the  grain  again  becomes  finer  (845),  the  pinkish  felspar  at 
the  same  time  increasing  in  amount,  and  occurring  to  some  extent  in  a  por- 
phyritic  manner, 170 

4.  Covered,  by  water, 250 

5.  Hornblende  rock  (846):    very  fine-grained,  highly  crystalline,  distinctly  bed- 

ded; in  places  thin  bedded;  dark-colored  or  black;  strike  N.  60°  E.,  dip 
60°S.E.,  20 

6.  Covered,  on  islands    70 

7.  Hornblende  rock:    similar  to  the  last  described,  but  much  weathered  and 

broken  by  joints;  strike  and  dip  obscure . .        20 

S.  Covered    35 


THE  ARCHAEAN  ROCKS. 


9.  Red  granite  (847):  medium-grained,  structureless,  pinkish  to  red,  highly  fels- 

pathic.     By  following  the  strike 


Feet. 


FIG.  7. 


JUNCTION  OF  GRANITE  AND  HORNBLENDE  ROCK. 
Scale  100  feet  to  the  ineh. 


directions  south-westward  for 
some  hundreds  of  feet,  the  junc- 
tion between  this  and  the  preced- 
ing dark-colored  rock  is  found 
on  a  large  water-worn  surface 
near  the  dam  at  the  Grand  Ra- 
pids foundry.  Here  the  two  rocks 
are  seen  to  interlock  in  a  curious 
manner,  the  granite  occurring 
in  large  masses,  entirely  sur- 
rounded by  the  other  rock.  The 
contrast  between  the  bright  red 
color  of  one,  and  the  black  of 
the  other,  makes  their  irregular 
junction-line  very  marked.  Fig. 

7  shows  this  junction  line.      Fig. 

8  is  the  part  of  Fig.  7,  at  A,  en- 
larged.     Where   the    sketches 
were  taken  the  granite  (894)  is 


10. 


somewhat  deeper  red  in  color  and  of  coarser  grain  than  on  the  line  of  sec- 
tion, its  deep  red  color  being  due  to  the  abundance  of  red  felspar,  which  is 
sometimes  in  facets  %  inch  in  diameter,  and  is  blotched  with  large  patches 
of  translucent  quartz.  The  rock  is  a  very  handsome  'one,  and  would  have 

value  as  an  ornamental  building  stone 35 

Hornblende    rock    (848) : 

FIG.  8. 


rather  fine-grained, 
,  highly  crystalline,  dark 
colored;  strike  and  dip 
obscure.  Hornblende 
and  a  whitish  felspar  ap- 
pear to  be  the  main  in- 
gredients. Magnetite  is 
present,  and  with  a 
magnifier,  can  be  seen 
in  bright,  metallic  par- 
ticles. Quite  coarse 
fragments  are  held  up 
by  the  magnet.  At  100 
feet  this  rock  becomes 
very  fine-grained  (849), 
and  rises  into  large  exposures,  over  which  the  dip  needle  stands  vertical. . . 

11.  Red  granite  (850):  moderately  coarse,  pink  to  red;  weathered  surface  bright 

red;  much  jointed;  no  bedding;  similar  to  No.  9.  The  mica  in  this  rock  is 
very  subordinate,  and  in  patches  of  small  flakes;  the  quartz  is  hyaline,  in 
considerable  blotches  of  granular  appearance;  the  felspar  is  pink  to  red, 
bright-lustred,  large-surfaced,  and  very  abundant 

12.  Hornblende  rock:   fine  grained,  dark- colored,  much  jointed;  strike  and  dip 

obscure 


ENLARGEMENT  OP  PORTION  OF  FIG.  7. 
Scale  4  feet  to  the  inch. 


120 


57 


58 


474 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


13.  Gneiss:  first  4  feet  is  coarse-grained,  pinkish,  and  quartzose  (851),  resem- 
bling that  at  beginning  of  section.  This  grades  into  a  light-gray,  coarser 
kind,  which  has  a  very  jagged  fracture,  is  less  micaceous,  shows  whitish 
felspar  predominating  over  pink,  and  only  obscure  lamination,  and  is  much 
cross-jointed  (853).  At  100  feet  the  bedding  becomes  distinct,  the  strike  be- 
ing N.  85°  E.,  the  dip  52°  S.  E.  At  230  feet  the  strike  is  N.  85°  E.,  the  dip 
50°  S.  E.,  the  rock  (854)  being  coarsely  mottled  gneiss  with  much  greenish 
mica  and  large-faced  reddish  felspar.  At  280  feet  the  bedding  is  the  same, 
and  a  small  red  felspar  vein  occurs.  At  300  feet  the  strike  is  N.  70°  E.,  the 
dip  55°  S.  E.  A  fine-grained,  red  granite  vein  occurs  here  having  the  form 
indicated  in  Fig.  9. 

FIG.  9. 


Feot. 


GRANITE  VEIN  AT  GBAND  RAPIDS. 

At  340  feet  the  bedding  and  lamination  of  the  rock  become  obscure  again 
and  continue  so  for  a  hundred  feet.  At  360  feet  numerous  thin  veins  of 
quartz  occur,  and  at  380  feet  one  of  pure  white  quartz  4  feet  wide.  At  420 
feet  are  some  large  veins  of  red  granite.  One  of  these  is  figured  in  Fig.  9. 
At  440  feet  the  bedding  becomes  plain  again,  the  strike  being  N.  85°  E.  and 
dip  as  before.  The  rock  here  (856)  is  much  less  micaceous  and  more  fels- 
pathic  than  for  some  distance  back,  and  is  much  weathered 494 

14.  Covered 190 

15.  Granite:  pinkish,  jointed,  without  indications  of  bedding 40 

16.  Gneiss:  dark-colored;  at  40  feet  this  changes  to  a  rock  (858)  which  closely 

resembles  that  at  the  close  of  3  (856),  and  is  moderately  coarse,  not  very  dis- 
tinctly gneissoid,  with  much  hyaline  quartz  and  large-faceted  felspar.  At 
60  feet  a  granite  vein  50  feet  long  occurs  in  this  rock,  coinciding  with  the 
bedding,  and  striking  N.  75°  E.,  with  a  dip  50°  S.  E.  The  vein  matter 
(859)  is  a  rather  fine-grained,  pinkish-red  granite,  weathering  dirty  brick- 
red,  and  showing  in  places  a  partial  kaolinization.  Fine  grained  translucent 
quartz  and  pinkish  felspar  make  up  most  of  this  granite.  Mica  is  present, 
but  in  very  small  quantity 130 

17.  Covered 30 

18.  Gneiss:  gray,  with  much  black  mica,  similar  to  that  of  16  (858).    At  10  feet 

a  granite  vein  2  feet  wide  occurs,  coinciding  with  the  bedding,  which  here 
shows  a  strike  of  N.  73°  E.,  and  a  dip  55°  S.  E.  Other  smaller  granite  veins 
occur.  Junction  with  the  next  rock  concealed 100 


THE  ARCH.EAN  ROCKS. 

19.  Hornblende  rock  (859%);  very  fine-grained,  highly  crystalline,  dark  green- 

ish-black; contains  much  of  a  highly  lustrous  bLick  mineral  (hornblende) , 
pyritiferous;  adheres  slightly  to  the  magnet  in  a  fine  powder.  See  also  Mr. 
Wright's  microscopic  examination,  Appendix  B 

20.  Gneiss:  resembling  that  of  18;  at  first  obscurely  bedded,  then  at  60  feet 

more  distinctly  bedded,  the  strike  being  N.  75°  E.,  and  the  dip  53°  S.  E. 
At  100  feet  3  granite  veins,  each  3  inches  thick,  occur 

21.  Covered 

FIG.  10. 


475 

Feet. 


120 
40 


GRANITE  VEIN  IN  GNEISS  AT  GRAND  RAPIDS. 

22.  Granite:  fine-grained,  light  pinkish,  slightly  gneissoid;  jointed.  The  three 
ingredients  are  all  perceptible  with  a  magnifier.  The  mica  shows  some 

tendency  to  a  stringy  arrangement 80 

S3.  Covered 45 

24.  Granite :  same  as  last  described 35 

25.  Hornblende  rock:  strike  N.  85°  E.,  dip  75°  S 10 

26.  Covered 150 

27.  Granite :  pinkish,  gneissoid 50 


Total  horizontal  length  of  section 2, 519 

Approximate  thickness  of  rocks  exposed 2, 200 


From  the  foregoing  details  we  may  construct  the  generalized  section  of  Fig.  11,  the  red 
granite  of  portions  of  the  section  being  regarded  as  an  intrusive  rock. 

At  the  first  dam  below  the  wagon  bridge  at  Centralia,  on  the  west  side  of  the  river, 
a  ledge  of  hornblende  rock,  40  feet  wide,  occurs.  This  rock  (884)  is  moderately  coarse- 
grained, dark-colored  to  black,  and  appears  to  be  composed  of  hornblende  and  a  white 
felspar  with  much  magnetite,  the  latter  very  distinctly  visible,  by  the  aid  of  the  magni- 
fier, in  lustrous  grains.  Quite  coarse  pieces  are  lifted  by  the  magnet.  On  the  river 
bank  a  short  distance  up  stream,  micaceous  gneiss  is  exposed,  forming  apparently  the 
next  layer.  These  beds  are  higher  in  the  series  than  any  of  those  in  the  section  at  the 
rapids. 

At  the  pail  mill,  just  below  Centralia,  is  a  large  exposure  of  fine-grained,  pinkish, 
gneissoid  granite,  containing  much  reddish  felspar,  and  fine,  glistening,  greenish  mica, 
with  a  stringy  arrangement. 


476 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


On  the  N.  W.  qr,  of  Sec.  5,  T.  22,  R.  6  E.  (point  D  of  map),  on  the  west  side  of  the 
Wisconsin,  kaolin  occurs  on  the  land  of  Mr.  C.  B.  Gar- 

g  s  "g  rison.    The  clay  here  is  reached  about  18  inches  to  2)-^ 

"2^  feet  below  the  surface,  and  has  been  exposed  in  places 

tC-<jI 

"§•*•«  for  a  distance  of  some  rods,  by  "  borrowing : '  for  the 

v'z.^  railroad   near  by.     Several  grades  are  to  be  seen.     lu 

Sis  3  some  places  the  spade  turns  up  a  brilliant  white  article; 

K  Co  in  others,  for  the  most  part  nearer  the  surface,  a  kind 

.•§!?§  that  is  largely  stained  with  the  brown  oxide  of  iron; 

g*^  whilst  at  others  again,  the  lamination  of  the  unaltered 

i  z  ,5  rock  is  still  distinctly  perceptible  in  the  soft  clay,  in 

ItsT-;  which  cases  it  is  more  apt  to  show  a  slight  bluish  cast, 

•g  | «»  and  many  silvery  mica  scales.    All  of  the  clay  is  quite 

"8  °*.2  gritty  from  the  presence  of  undecomposed  felspar  and 

(.5 1  quartz  grains.     Rounded,  reddish  quartz  pebbles  up  to 

^  a  so  i^/  inch,  in  diameter,  are  occasionally  to  be  seen.    TLo 

g<-g  depth  of  the  clay  at  this  place  is  said  to  be  at  times  as 

.§  5  "3  much  as  4  feet.     Samples  of  the  wlu'test  kinds  yielded 

§       ^'«3>  the  following  results: 

807  A. 

*  j|l'       Silica 78.83 

§  JUlw  Alumina..                       .  13.43 


Iron  oxyd 
Lime 

Magnesia . 
Potash... 
Soda 


SO  7  -B 

49.94 
36.80 
.72 
trace 


Water 5.45 


99.60 

Carbonic  acid 01 

Specific  gravity 2.52 


.51 

.08 

11.62 

99.67 


2.52 


soy  c 
92.86 
2.08 
.74 
.96 
.10 
.28 
.05 
2.53 

99.60 


S±>* 


807  A  is  the  raw  clay  dried  at  100°  C.;  807  B  is  the 
fine  clay  obtained  from  A  by  repeated  stirrings  and 
washings;  807  C,  the  coarse  residue  from  the  washing. 
The  composition  of  this  residue  is  calculated  from  the 
two  preceding  analyses.     Under  the  microscope   it    is 
seen  to  consist  chiefly  of  angular  fragments  of  quartz 
from  Tfa  to  aV  inch  in  diameter,  mingled  witli  very  fine 
fragments  of  felspar.    The  approximation  in  composi- 
tion of  the  roughly  washed  fine  clay  to  typical  kaolinite 
|  7  ^  g    is  noteworthy.    The  unwashed  kaolin  (A)  is  composed 
*  of  32.7  fine  clay  (B),  and  67.3  coarse  residue  (C).    The 
following  are  the  compositions  of  B  and  C  expressed  in 
I   percentages  of  the  unwashed  clay  (A).    The  manner  of 

•   •  *  distribution  by  washing  of  the  various  ingredients  of  the 

raw  clay  is  thus  indicated,  and  the  practical  advantage  to  be  obtained  by  washing 
shown: 


r;  a  o  <a 
S.HM  H 


THE  ARCHAEAN  ROCKS.  477 

tSO7  B  8O7  C  807  A 

Silica 16.33  4-  62.50  =  78.83 

Alumina 12.03  -t-  1.40  =  13.43 

Iron  oxide 24  +  .50  =        .74 

Lime 00  +  .64  =        .64 

Magnesia 00  -r  •     .07  =        .07 

Potash 12  +  .25  =        .37 

Soda 03  +  .04  =        .07 

Water 3.75  +  1.70  —  5.45 


32.50     +     67.10    =    99.60 


The  most  ferruginous  clays  seen  at  Mr.  Garrison's  yielded  1.68  per  cent.  (808),  and 
2.31  per  cent.  (809)  of  iron  sesquioxide.  These  are  apparently  much  more  plenty  than 
the  white  clay.  About  10  rods  from  the  kaolin  openings,  on  the  river  edge,  is  a  low 
outcrop  of  a  highly  micaceous,  weathering  gneiss  (803).  having  a  moderately  coarse, 
jagged  texture.  The  felspar  of  this  rock  is  largely  still  brilliant,  but  little  white  kaolin 
patches  dot  the  surface.  Another  outcrop  near  by  shows  a  more  highly  felspathic  kind, 
with  very  coarse,  pinkish  orthoclase.  These  gneisses  closely  resemble  the  prevailing 
ones  in  the  Grand  Rapids  section,  but  are  evidently  much  lower  in  the  series  than  any 
of  those. 

At  the  Green  Bay  and  Minnesota  depot,  Grand  Rapids,  it  is  reported  that  in  excavat- 
ing for  a  turn-table,  first  a  few  layers  of  compact  sandstone  were  penetrated,  then  5  to 
6  feet  of  soft  white  clay  and  decomposed  rock.  Near  the  center  of  Sec.  4,.T.  22,  R.  6  E. 
(point  E  of  map),  about  two  miles  above  Grand  Rapids,  on  the  east  bank  of  the  Wis- 
consin, on  Mr.  Rablin's  land,  very  white  kaolin  shows,  overlaid  by  two  feet  of  sand- 
stone. This  kaolin  has  been  used  with  success  to  line  the  furnaces  at  the  Grand  Rapids 
foundry.  The  following  are  analyses  of  samples  from  here : 

829  828 1-2 


A.  JB  B 

Oxide  of  iron 4.43 

Potash 1.21  .87  .38 

Soda .46  .08 


829  A  and  829  B  are  raw  and  washed  clay  taken  from  the  stock-pile  at  the  foundry ; 
828%  is  washed  from  a  sample  taken  from  the  opening  itself. 

On  the  line  of  the  Wisconsin  Valley  Railroad,  between  Centralia  and  Junction 
City,  are  several  low  cuttings,  which  expose  usually  crumbling,  and  partially  decom- 
posed, laminated  gneiesic  rocks.  The  exposures  are  very  poor  and  the  rock  is  generally 
out  of  position.  About  3%  miles  north  of  Centralia  is  a  cutting  400  feet  long,  through 
a  rather  fine-grained,  granular  textured,  pinkish  granite  (965).  This  rock  consists  of 
brownish,  translucent,  granular,  glassy  quartz,  largely  predominating;  pinkish  bright- 
lustered  felspar;  and  fine  black  mica  sparsely  but  uniformly  scattered.  It  would  dress 
readily,  but  shows  some  tendency  to  weather  and  iron  stain. 

West  of  the  railroad  line,  in  the  western  part  of  T.  23,  R.  6  E.,  sandstone  occurs  in 
places,  sometimes  capping  the  hills,  sometimes  low  in  the  valleys,  and  lying  evidently 
upon  a  very  irregular  crystalline  rock  surface.  On  Sec.  8,  near  the  northwest  corner  of 
the  section,  a  well  passes  through  sand  6  feet,  sandstone  2%  feet,  soft  red  and  white 
kaolinized  rock  20  feet.  This  is  the  greatest  depth  of  softened  rock  that  has  come  to  my 
notice  in  Wisconsin. 


478 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


FIG.  12. 


At  Conant's  Rapids,  sections  18  and  17,  T.  23,  R. 
8  E.,  Portage  county,  are  large  rock  exposures  in  the 
"bed  and  on  the  sides  of  the  Wisconsin  river.  The 
sketch-map,  Fig.  12,  shows  the  localities  of  the  occur- 
rences at  this  place,  as  also  at  the  Stevens  Point  rap- 
ids, above. 

On  the  west  side  of  the  river  the  rock  exposures  and 
rapids  are  found  continuing  further  down  stream  than 
on  the  east,  on  account  of  the  northeast  strike  of  the 
rocks.  Beginning  at  the  foot  of  the  rapids  on  the 
west  side,  we  note  first  on  the  N.  W.  qr.  of  the  N.  E. 
qr.  of  Sec.  17,  a  low  exposure  some  500  feet  in  length, 
under  the  river  bank,  No.  I  of  map.  The  rock  here 
(775)  is  a  fine-grained,  pinkish-gray  gneiss,  showing 
fine-granular,  translucent  quartz,  predominating;  fine- 
faceted  white  felspar,  abundant;  black  mica  in  very 
fine  separate  scales,  arranged  in  lines.  The  lamina- 
tion is  quite  close  and  distinct.  The  weathered  sur- 
face of  the  exposure  is  brownish  in  color,  smooth,  ana 
highly  polished  by  the  running  action  of  the  river 
From  this  smoothed  and  brown- tinted  surface  numer- 
ous reddish  granite  veins  stand  out  in  bold  relief,  hav- 
ing resisted  the  eroding  action  more  successfully  than 
the  suiTOunding  rock.  The  bedding  is  not  very  dis- 
tinct, being  obscured  by  many  cross-joints;  the  strike 
is  N.  81°  E.,  and  the  dip  N.  W.  60°  to  67°.  Other 
quite  prominent  joints  occur,  bearing  N.  55°  E.,  and 
standing  vertical.  Numerous  veins  are  to  be  seen 
here,  both  of  white  quartz,  and  of  reddish  felspathic 
granite,  varying  in  thickness  up  to  several  inches. 
One  granite  vein  5  inches  wide  trends  N.  26°  E.,  for 
a  distance  of  50  feet.  The  vein  matter  (775)  is  a  very 
fine-grained  felspathic  granite,  in  which  all  the  ingredients  can,  however,  be  distin- 
guished. Numerous  thin  feeders  extend  from  the  vein  into  the  rock  around.  The  next 
exposure  above,  No.  II  of  the  map,  is  a  large  one,  stretching  across  a  side  channel  of  the 
river,  just  about  on  the  line  beetween  sections  8  and  17.  The  rock  here  (778)  is  a  very 
coarse-grained,  micaceous,  granite,  consisting  of  very  large-flaked  brilliant  black  mica; 
white,  very  distinctly  striated  felspar,  in  facets  up  to  %  inch  by  %  inch  in  size;  limpid 
quartz;  some  brownish- stained  mica;  and  some  little  hornblende.  In  some  places  a 
very  distinct  tendency  to  crumble  is  perceptible,  and  then  the  mica  is  much  iron-stained, 
and  the  rock  is  blotched  with  large  patches  of  white,  kaolinized  felspar.  Even  where 
exposed  to  the  running  water  this  rock  presents  nowhere  the  peculiar  smoothed  and 
glistening  appearance  of  the  exposure  below,  but  on  the  contrary  shows  everywhere  a 
rough,  coarsely  pitted  surface.  This  is  rendered  the  more  striking  by  the  innumerable 
reddish  granite  and  white  quartz  veins  which  intersect  the  rock  in  every  direction,  mak- 
ing up  nearly  half  of  the  exposure,  for  these  having  resisted  better  the  weathering  in- 
fluences, show  the  smoothed  appearance  alluded  to,  and  stand  out  in  relief  from  the 
lighter  colored,  jagged  surface  of  the  surrounding  rock.  The  veins  are  from  1  inch  to  18 
inches  in  width.  The  reddish  ones  are  of  granite,  having  a  large  predominance  of  red- 
dish felspar,  which,  in  some  of  them,  occurs  along  the  sides  of  the  vein  free  from  ad- 
mixture, and  in  large  crystalline  surfaces.  One  vein  2^  inches  wide  showed  alternating 
bands  of  white  quartz,  pink,  coarsely  crystalline  felspar,  and  felspathic  granite  (777). 


SKETCH-MAP  SHOWING  LOCALITIES 
OF  HOCK  EXPOSURES  AT  CONANT'S 
RAPIDS  AND  STEVENS  POINT  RAP- 
IDS. 

Scale,  one  mile  to  the  inch. 


THE  ARCHJEAN  ROCKS. 


479 


Exposure  No.  Ill  of  the  map  is  on  the  road  side  in  the  S.  W.  qr.  of  the  S.  E.  qr.  of  Sec. 
8.  The  rock  here  is  a  fine-grained,  light-pink,  gneissoid  granite  (779),  having  the  three 
ingredients  distinctly  visible,  though  fine,  and  showing  a  few  whitish  kaolinized  patches. 
At  No.  IV  of  the  map,  are  large  exposures  at  the  top  of  the  bank  and  in  the  river  be- 
low. Fig.  13  shows  the  occurrences. 

FIG.  13. 


WfSt          '': 


^^^•^•^;;^^^'^^^-^ 
'-  '*''<;r' 


Scale,  30  feet  to  the  inch. 

At  A  is  a  bold  exposure  of  smooth-jointed,  fine-grained,  light-reddish  granite  (780),  in 
which  red-stained  granular  quartz  is  the  predominating  ingredient,  mica  being  very 
subordinate,  occurring  in  fine  brilliant  brownish  flakes,  and  showing  a  slight  tendency 
towards  a  stringy  arrangement.  The  numerous  joints  which  traverse  this  rock  strike 
N.  17°  W.,  and  stand  nearly  vertical.  At  B  (782)  is  a  coarse-grained,  red-and-black- 
mottlcd,  micaceous  gneiss,  striking  plainly  N.  59°  E.  This  rock  resembles  that  of  No. 
Ill,  but  contains  much  more  reddish  non-striated  felspar.  Whitish  kaolinized  patches 
occur.  Bounding  this  on  the  south,  at  C,  and  sharply  defined  from  it,  is  a  fine-grained, 
dark-greenish  crumbling  rock  (781),  having  a  marked  E.  W.  lamination.  This  rock 
appears  to  contain,  predominatingly,  fine  blackish  mica,  with  which  appears  to  be  min- 
gled some  fine  whitish  felspar  (mica-schist?).  Little  pinkish  felspathic  threads  traverse 
the  rock.  To  the  south  of  this  again,  at  D,  comes  in  a  fine-grained,  very  compact, 
greenish,  gneissoid  granite  (783),  striking  N.  70*  E.  and  showing  as  constituents,  fine- 
flaked,  blackish  mica,  pink  and  white  felspar,  and  limpid  quartz. 

Passing  now  to  the  east  side  of  the  river,  we  note  first  on  the  N.  E.  qr.  of  the  S.  E. 
qr.  of  Sec.  8,  near  the  foot  of  the  rapids,  and  just  above  the  mouth  of  Plover  river, 
at  No.  V  of  the  map,  large,  but  low,  outcrops  of  quartzose  gneiss,  bearing  nearly 
east  and  west,  dipping  south  60*,  and  overlaid  by  25  to  35  feet  of  horizontal  sandstone. 
This  point  appears  to  be  on  the  anticlinal  line  where  the  southeast  dips  of  the  Grand 
Rapids  series  give  place  to  the  northeast  dips  of  the  Conant's  and  Stevens  Point 
rapids. 

On  the  N.  E.  qr.  of  the  N.  W.  qr.  of  the  same  section  (No.  VI  of  map),  large  ex- 
posures begin,  which  extend  up  stream  for  a  long  distance,  and  show  all  along  a  very 
marked  trend  of  N.  25°  E.  The  southernmost  rock  examined  here  is  a  fine-grained, 
dark-colored,  highly  micaceous  gueiss,  traversed  by  numerous  large  veins  of  reddish 


480 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


FIG.  14. 


granite  aiid  smaller  ones  of  white  quartz.     In  some  of  the  veins,  quartz,  felspar,  and 
granite  all  occur  separately,  as,  for  instance,  in  the  one  shown  in  Fig.  14. 

The  vein  rock  here  '799^)  is  a  fine-grained 
admixture  of  quartz  and  pinkish  felspar,  mica 
being  almost  wholly  absent.  The  vein,  and  its 
ramifications  as  well,  are  sharply  defined  from 
the  wall  rock.  A  short  distance  up  stream  from 
this  vein  the  gneiss  shows  an  exceedingly  fine 
lamination,  and  becomes  much  contorted  (799). 
.  The  lamination  is  due  in  part  to  a  general 
stratified  structure  of  the  rock,  independently  of 
its  ingredients,  but  in  part,  also,  to  an  aggre- 
gation of  the  fine  black  mica  along  the  surfaces 
of  laminae .  The  ingredients  of  the  rock  are  fine  - 
grained,  colorless  quartz,  predominating;  coars- 
er, pinkish,  translucent  quartz;  black,  shining, 
small-flaked  mica,  very  abundant;  and  small-fa- 
ceted, white  felspar.  The  exposure  of  contorted 
gneiss  is  quite  abruptly  limited  up  stream,  by 
a  large,  pinkish  granite  mass,  which  stands  6  to 
10  feet  above  the  surrounding  rock  at  No.  VII 
of  the  map.  The  rock  of  this  large  vein  (798)  is 
similar  to  that  of  the  vein  last  described,  but  is 
somewhat  more  quartzose.  Next  above  the 
granite  vein  is  a  fine-grained,  fclspathic  gneiss 
(797),  striking  N.  35°  E.,  dipping  80°  N.  W., 
and  intersected  by  numerous  cross-joints.  Next 
above  this  are  again  high  exposures  of  fine- 
grained, structureless,  pinkish  granite  (796),  re- 
sembling the  masses  and  veins  further  down, 
but  much  larger  in  size. 

At  VIII  of  the  map,  fine-grained,  greenish- 
brown  gneiss  (795)  is  exposed,  striking  N.  50° 
E.,  and  dipping  45°  N.  W.,  and  composed  of 
silvery  mica,  pinkish  felspar,  and  translucent 
quartz.  A  short  distance  above,  this  grades 
into  a  coarser  kind  (794),  which  is  very  plainly 
laminated,  in  places  even  schistose,  and  carries 
small  greenish  epidote(?)  veins. 

In  the  Rapids  at  Stevens  Point,  on  Sees. 
32  and  31,  T.  24,  R.  8  E.,  are  some  considera- 
ble exposures,  which  are,  however,  not  so  large 
as  those  at  Conant's  Rapids,  a  mile  below. 
The  localities  of  the  main  outcrops  in  the  Ste- 
vens' Point  Rapids  are  shown  on  the  map,  Fig. 
12.     At  the  point  IX  of  the  map,  on  the  south 
y  line  of  Sec.  32,  is  a  low  exposure,  at  the  water's 
GRANITE  VEIN  AT  CONANT'S  BAPIDS.  erige> of  a  moderately  course,  laminated,  brown- 

Scale  6  feet  to  the  inch  ish-stained  micaceous  gneiss  (785),  striking  N. 

45°  E.,  and  dipping  70°  to  80°  N.  W.    This 

rock  is  composed  of  abundant  brilliant  black  mica,  which  weathers  brownish;  coarse 
faceted,  plainly  striated,  white  felspar;  and  limpid  quartz.    The  weathered  surface  is 


Granite       Quartz 


THE  ARCHAEAN  ROCKS.  43  j 

dark-brownish,  and  rough,  and  has  underneath  a  whitish  kaolinized  crust.  Throughout 
small  white  kaolin  patches  occur.  This  rock  closely  resembles  that  on  the  west  side  of 
Conant's  rapids  (778).  In  the  bank  above,  sandstone  is  exposed. 

Under  the  central  abutment  of  the  railroad  bridge,  and  about  100  feet  northwest  from 
the  exposure  last  described,  occurs  another  of  the  same  rock,  but  somewhat  coarser  and 
less  predominatingly  micaceous.  The  bedding  is  the  same  as  before. 

About  300  feet  further  across  the  strike,  and  now  on  the  west  side  of  the  river,  point 
X  of  map,  is  a  large  exposure  of  the  same  mottled  micaceous  gneiss,  extending  several 
hundred  feet  along  the  river  bank.  At  the  lower  end  of  the  exposure,  the  felspar  sur- 
faces are  very  large  and  very  finely  striated  (787),  and  the  rock  is  more  weathered  than 
usual,  the  ordinarily  brilliant  black  mica  being  largely  changed  to  a  brownish  tint, 
which  affects  the  appearance  of  the  whole  rock.  Reddish  veins,  composed  almost  en- 
tirely of  coarse,  cleavable  felspar,  occur,  and  also  others  in  which  the  felspar  is  coarsely 
mingled  with  wlu'te  quartz.  The  character  of  the  rock  remains  the  same  throughout 
the  length  of  the  exposure,  as  far  north  as  the  wagon  bridge,  the  bedding  throughout 
being  very  distinct,  and  showing  a  strike  of  N.  75°  E.,  and  a  dip  of  45°  N.  W.  A  short 
distance  west  from  the  river  bank,  at  this  place,  horizontal  sandstone  is  exposed  in  the 
railroad  cutting  and  in  a  large  quarry. 

The  crystalline  rock  series  at  Conant's  rapids  and  Stevens  Point  may  be  briefly  de- 
scribed as  consisting  of  beds  of  highly  micaceous  gneiss,  dipping  northwest  from  45° 
to  80°,  trending  N.  25°  to  N.  65°  E.,  with  which  are  interstratified  some  layers  of  a 
finer  grained,  less  micaceous  gneiss,  and  penetrating  which  are  reddish  granite  veins 
and  masses.  Compared  with  the  gneisses  of  Grand  Rapids,  those  just  described  are 
found  to  be  more  highly  micaceous  and  usually  coarser  grained.  They  differ  from  the 
Grand  Rapids  rocks  also  in  having  as  a  prominent  constituent  a  triclinic  (striated), 
whitish  felspar,  and  in  having  no  interstratified  beds  of  dark-colored,  fine-grained  horn- 
blendic  rocks.  The  Grand  Rapids  rocks  dip  southeastward,  those  of  Conant's  rapids 
and  Stevens  Point,  except  at  the  southernmost  point,  northwestward,  the  strikes  in 
both  cases  being  northeast,  but  not  always  equally  so.  The  anticlinal  line  cannot  be  far 
from  the  great  bend  and  long  southwestward  stretch  of  the  Wisconsin  in  southern 
Portage  and  Wood  counties,  and  to  this  anticlinal  line  the  peculiar  change  in  the  course 
of  the  river  evidently  bears  a  close  relation.  See,  in  this  connection,  Atlas  plate  XV  of 
Area  F,  and  its  accompanying  north  and  south  section. 

On  Plover  river,  in  the  N.  E.  qr.  of  Sec.  12,  T.  24,  R.  8  E.,  three  quarters  of  a  mile 
north  of  Jordan,  is  a  low  ledge  of  moderately  coarse,  pinkish,  porphyritic  granite  (806). 
The  felspar  is  in  facets  up  to  %  inch  in  diameter,  both  white  and  pink,  the  former  finely 
striated;  the  quartz  is  both  hyaline  and  abundant;  the  mica  is  in  medium-sized,  brilliant, 
black  flakes.  Numerous  white  kaolin  patches  indicate  a  tendency  to  decompose. 

On  the  line  of  the  Wisconsin  Central  Railroad,  between  Stevens  Point  and  Junc- 
tion City,  are  several  small  rock  cuttings.  One  of  these,  on  Sec.  22,  T.  24,  R.  7  E.,  is 
in  a  pinkish,  fine-grained  granite  (800),  showing  pink  and  white  felspar,  quartz,  and 
fine  black  mica.  Another,  one  mile  below  Junction  City,  on  Sec.  1,  T.  24,  R.  6  E.,  is  in 
a  decomposing,  medium- grained  to  fine-grained,  whitish-weathering  gneiss  (801,  802, 
803,  804),  composed  chiefly  of  quartz  and  pinkish  felspar  in  blotches,  with  a  greenish, 
greasy  mineral  (chlorite  or  altered  mica)  on  surfaces  and  in  fine  strings  throughout. 
Pyrite  is  present,  and  white  kaolinized  blotches  are  characteristic.  The  more  decom- 
posed portions  show  a  schistose  tendency,  and  in  all  there  is  a  marked  parallel  grain. 
The  bedding  structure  shows  a  strike  of  N.  22°  E,  and  a  dip  of  80°  E.  These  are  also 
the  directions  of  the  grain  of  the  rock.  On  Sec.  2,  half  a  mile  from  Junction  City,  is  a 
small  exposure  of  a  decomposed  brick-red,  ferruginous,  schistose  gneiss  (805),  showing 
nn  the  interior  numerous  shining  mica  flakes,  but  too  far  altered  to  show  any  other 
minerals. 

Wis.  SUR.  — 31 


482  GEOLOGY  OF  CENTRAL  WISCONSIN. 

On  the  line  of  the  Wisconsin  Valley  Railroad,  between  Junction  City  and 

Knowlton,  there  are  numerous  small  rock  cuttings,  chiefly  in  more  or  less  decomposed 
gneissic  and  scliistose  rocks.  The  drift  along  the  line  is  very  light,  and  every  little  cut- 
ting exposes  the  rock.  Half  a  mile  north  of  Junction  City,  in  the  north  part  of  Sec.  2,  T. 
24,  R.  6  E.,  small  exposures  are  seen  for  a  distance  of  300  feet,  of  much  decomposed,  fine- 
grained, dark-colored  mica-schist  or  micaceous  gneiss.  A  similar  rock  shows  a  quarter 
of  a  mile  further  north,  on  Sec.  35,  T.  25,  R.  6  E.  Here  the  rock  is  a  fine-grained,  very 
closely  laminated,  blackish  schist  (963).  The  predominating  black  mineral  is  partly  horn- 
blende, partly  mica.  In  the  north  part  of  Sec.  35,  \%  miles  from  Junction  City,  a  cut- 
ting shows  for  50  feet  at  its  south  end  a  blackish  schist,  similar  to  the  last  described,  in 
all  stages  of  decomposition,  even  to  a  light  colored  clay.  The  lamination  lines  are 
marked,  and  bear  N.  50°  E.  At  the  north  end  of  the  cut  a  decomposing,  fine  grained, 
arenaceous,  light-colored  schist  (962)  is  exposed,  composed  apparently  chiefly  of  fine 
granular  quartz.  On  some  of  the  laminse  light-colored,  altered  mica  is  perceptible. 
One-fourth  mile  further  north  is  a  small,  indefinite  exposure  of  the  same  arenaceous 
schist.  In  the  east  part  of  Sec.  26,  2%  miles  from  Junction  City,  the  railroad  cutting 
makes  an  exposure  200  feet  long  and  8  feet  high.  The  rock  (959,  960,  961)  is  a  fine- 
grained, dark-greenish  to  black,  calcareous  mica-schist,  or  gneiss,  showing  very  fine  and 
uncontorted  lamination,  and  a  peculiar  knotty  appearance  in  places  from  the  occurrence 
of  lumps  of  quartz  and  calcite  between  the  laminae,  which  are  then  bent  around  these 
nodules.  The  preponderating  black  mineral  is  in  fine  shining  scales,  and  appears  to  be 
chiefly  mica.  Veins,  j^  to  %  inch  in  width,  of  a  greenish,  translucent  mineral  (epidote?) 
occur.  The  lamination  of  the  rock  causes  it  to  break  out  in  columnar  forms,  some  of 
the  columns  reaching  a  size  of  8x4x4  feet.  The  apparent  dip  is  N.  N.  W.  85°.  A 
somewhat  similar  calcareous  gneiss  occurs  on  Black  river  in  Clark  county.  Three  miles 
from  Junction  City,  on  Sec.  24,  T.  25,  R.  6  E.,  is  a  small  exposure  of  a  fine-grained, 
white-weathering,  crumbling,  arenaceous,  talco-mica-schist  (858),  showing  very  fine 
lamination,  and  closely  allied  to  the  light-colored  rock  seen  in  the  cutting  \%  miles 
north  of  Junction  City.  "With  a  lens,  fine-grained  quartz  is  seen  to  be  the  predominat- 
ing constituent.  Half  a  mile  farther  north  is  an  indefinite  exposure  of  a  fine-grained, 
dark-colored  gneiss,  or  mica-schist,  similar  to  that  seen  in  the  large  cutting  on  Sec.  26. 
About  4  miles  from  Junction  City,  on  Sec.  13,  T.  25,  R.  6  E.,  light-colored,  fine-grained, 
arenaceous  mica-schist  (999)  is  again  exposed,  for  300  feet,  on  the  side  of  a  cutting. 
The  lamination  planes  strike  N.  30°  E.,  and  dip  80°  S.  E.  A  few  small  masses  of  milky 
quartz,  and  reddish  felspathic  veins  are  included,  and,  in  places,  stand  out  in  relief  from 
the  surrounding  decomposed  rock.  On  the  north  part  of  Sec.  13,  4%  miles  south  of 
Knowlton  bridge,  an  indistinct  exposure  of  pinkish,  weathered  granite  occurs.  Another 
indefinite  exposure  of  the  same  rock  occurs  a  quarter  of  a  mile  further  north,  on  Sec.  12. 
In  the  north  part  of  Sec.  12,  3.7  miles  south  from  Knowlton  bridge,  the  following  section 
occurs  in  a  low  cutting,  the  rock  exposures  not  rising  more  than  one  or  two  feet  above 
the  railroad  track,  and  being  considerably  out  of  position.  The  section  begins  at  the 
north  end  of  the  exposure: 

1.  Granite  (992):    very  fine-grained,  red  colored,  felspathic;  partly  kaolinized 

on  surface;  penetrated  by  veins  of  white  quartz 2 

2.  Decomposed  gneiss:    clayey;  containing  occasionally  seams  of  partly  kao- 

linized reddish  granite  (993) 50 

3.  Quartz:    white 1 

4.  Granite  (994):   partly  decomposed;  very  fine-grained;  granular,  pink  col- 

ored, quartzose;  crumbles  in  fingers  to  a  sand 3 

5.  Decomposed  gneiss:    clayey,  but  showing  still  a  distinct  contorted  lamin- 

ation       6 


THE  ARCILEAN  ROCKS.  483 

Ft     In. 

6.  Granite  (995) :  similar  to  No.  4;  holding  veins  .and  masses  of  quartz 10 

7.  Decomposed  gneiss :    similar  to  No.  5 20     . . 

8.  Granite :   light- pinkish,  felspathic 4 

9.  Decomposed  gneiss :   similar  to  No.  7 30 

JO.  Red  felspathic  seam :   altered;  standing  vertical 2 

11.  Dark-green  rock  (997) :    composed  almost  entirely  of  a  fine,  flaky  mineral, 

which  appears  like  an  altered  amphibole 5 

12.  Granite:  reddish;  resembling  No.  G 6 

13.  Decomposed  gneiss:  contorted ;  holding  seams  of  quartz  and  partly  altered, 

fine-grained  granite 75 

Total..  204    10 


At  the  south  end  of  the  railroad  bridge  at  Knowlton,  in  the  north  part  of  Sec.  29,  T. 
26,  R.  7  E.,  is  a  cutting  100  feet  long,  and  5  to  10  feet  deep,  through  rock.  The  northern 
portion  of  the  cut  exposes  a  fine-grained,  blackish,  hornblende  schist  (890),  having  a 
distinct  crystalline  texture,  and  resembling  much  some  of  the  hornblendic  beds  of  the 
section  at  Grand  Rapids.  The  apparent  strike  of  this  rock  is  N.  55°  W.,  and  the  dip 
60°  N.  E.  Its  horizontal  width  at  right  angles  to  this  strike  direction  is  about  40  feet. 
The  remainder  of  the  cut  is  in  modi  um*  grained,  highly  crystalline,  grayish,  granitoid 
rock  (889),  which  -weathers  white.  Quartz,  white  felspar,  and  dark-colored,  small-flaked 
mica,  the  latter  showing  a  slight  stringy  arrangement,  can  be  seen  with  a  Ions.  Some 
of  the  dark-colored  mineral  may  be  amphibole.  The  apparent  bedding  of  this  rock  co- 
incides with  that  of  the  preceding;  and  its  horizontal  width  is  also  about  40  feet. 

On  the  wagon  road  between  Knowlton  and  Mosinee,  on  the  east  side  of  the  Wis- 
consin, several  small  and  indefinite  exposures  occur  of  decomposing  fine-grained  rocks, 
resembling  those  observed  on  the  line  of  the  Wisconsin  Valley  Railroad.  Two  miles 
north  of  Knowlton,  where  the  road  ascends  a  high  ridge,  exposures  occur  of  a  fine- 
grained to  aphanitic,  dark  colored,  slaty  rock  (892.)  This  rock  is  pyritiferous,  and  dis- 
tinctly attracted  by  the  magnet  in  coarse  powder;  it  weathers  with  a  dirty- white,  earthy 
surface.  At  3.7  miles  north  of  Knowlton,  another  exposure,  of  a  similar  rock,  occurs  in 
the  road.  This  rock  (968),  according  to  Mr.  Wright's  microscopic  examination,  is  com- 
posed of  chlorite,  altered  felspar  and  magnetite.  These  exposures  were  all  too  poor  to 
show  any  definite  bedding  structure. 

At  Little  Bui)  falls,  on  the  Wisconsin  rivor,  at  Mosinee,  Sec.  29,  T.  27,  R.  7  E., 
Marathon  county,  are  quite  large  rock  exposures.  The  river  here  is  divided  into  twa 
widely  separated  channels  by  a  high  rocky  island  about  a  quarter  of  a  mile  in  width. 
On  its  northeast  end  tins  island  is  itself  cut  by  several  smaller  channels,  dry  at  low  water, 
which  show  high  walls  of  bare  rock.  Most  of  the  water  of  the  river  passes  through  tho 
easternmost  channel,  which  in  one  place,  for  a  distance  of  130  feet,  is  a  gorge  only  35 
feet  wide.  The  main  fall  of  the  river  was  formerly  in  this  gorge,  but  has  lately  been 
moved  down  stream  by  a  dam  erected  below.  The  rocks  of  the  various'  exposures  at 
this  place  aie  all  closely  allied  and  may  be  designated  by  the  general  term  of  syenite. 
They  axe  all  characterized  by  the  presence  of  much  greenish-black  amphibole,  and  white 
striated  felspar,  the  quartz,  though  present,  being  always  subordinate.  Two  general 
kinds  were  noted.  The  prevailing  rock  (8%,  898,  900)  is  a  moderately  coarse-grained, 
highly  crystalline,  syenite,  with  a  greenish-gray,  mottled  appearance,  and  without 
any  sign  of  parallel  arrangement  of  the  various  ingredients,  which  are  uniformly 
intermingled.  On  a  weathered  surface  this  rock  appears  greenish  to  white,  the 
latter  color  being  due  to  a  kaolinization  of  the  felspar.  On  a  fresh  fracture  the  two 
main  ingredients  are  readily  perceptible  to  the  naked  eye.  The  hornblende  is  usually 
of  a  bright-knitted,  greenish- black  color;  the  felspar  facets  are  commonly  white 


484  GEOLOGY  OF  CENTRAL  WISCONSIN. 

translucent,  and  beautifully  striated,  as  can  readily  be  seen  with  an  ordinary  lens.  More 
rarely  pinkish  felspar  occurs.  That  variety  of  this  rock  which  has  a  medium  degree 
of  coarseness  presents  a  very  handsome  appearance  on  a  dressed  surface;  and,  since 
it  shows  no  tendency  to  iron  -  stain  or  decompose,  might  make  a  valuable  building 
stone.  The  second  variety  found  here  (897,  905,  903)  is  very  much  finer  in  grain,  and  of 
a  dark. greenish-gray  color,  showing  the  crystalline  texture  only  under  the  lens,  and 
then  not  plainly.  It  is  evidently  merely  a  phase  of  the  coarser  rock.  It  occurs  both 
in  small  imbedded  patches  (879)  and  in  large,  distinct  outcrops  (905,  903).  According 
to  the  microscopic  examination,  these  finer  kinds,  whilst  having  the  same  ingredients  as 
the  coarser,  show  a  larger  proportion  of  hornblende,  and  may  be  designated  as  "  horn- 
blende rock."  Chlorite  appears  to  occur  in  all,  more  especially  in  the  finer  kinds,  as  an 
accessory. 

For  the  most  part  the  bedding  of  the  Little  Bull  rocks  is  indistinct.  In  two  places, 
however,  it  is  plainly  to  be  seen.  One  of  these  is  on  the  west  wall  of  a  dry*  side  chan- 
nel near  the  head  of  the  main  island.  Here  very  marked  planes  dipping  27°  S.  W.  and 
striking  N.  5°  W.,  are  to  be  seen  along  a  perpendicular  exposure,  20  feet  in  height  and 
50  in  length,  of  the  prevailing  coarse  syenite.  .  Across  the  bedding  lines  run  a  number 
of  joints  bearing  N.  42°  W.,  and  dipping  87°  S.  W.  The  other  place,  distant  from 
here  800  feet  in  a  nearly  due  south  direction,  is  on  the  same  island,  and  on  the  west  side 
of  the  east  or  main  channel,  just  below  the  dam.  Here  are  a  number  of  distinct  layers 
of  the  finer  grained  rock  (903),  averaging  14  inches  in  thickness,  and  dipping  20*  E., 
with  a  north  and  south  strike.  We  have  thus  indications  of  a  low  anticlinal,  whose 
nearly  north  and  south  axis  runs  diagonally  across  the  island,  and  nearly  in  the  direction 
of  the  river  above. 

On  the  large  exposure  mentioned  as  showing  a  westward  dip,  the  bedding  planes  are 
cut  by  a  vertical  north  and  south  vein  of  fine-grained,  dark-colored,  brown-weathering, 
hornblendic  rock  (899),  which  is  itself  traversed  and  partly  faulted  by  joints  that  affect 
it  and  the  wall  rock  alike.  Several  large,  white  quartz  veins  show  under  the  bridge 
across  the  first  dry  channel  west  of  the  main  gorge.  One  of  these  bears  N.  40°  E., 
dips  17°  N.  W.,  is  five  feet  wide,  and  composed  of  parallel  bands  a  quarter  of  an  inch 
to  three  inches  in  width.  A  still  larger  one  occurs  at  the  bottom  of  the  gorge,  where  it 
stands  out  very  prominently,  the  surrounding  rock  having  been  worn  away  by  the  run- 
ning water.  The  wall  rock,  seen  in  only  one  place,  is  fine-grained,  schistose,  dark- 
greenish,  and  apparently  chloritic  (902).  It  would  seem  to  be  an  advanced  stage  of  al- 
teration of  the  normal  amphibolic  rock  of  the  vicinity.  A  less  advanced  alteration  is 
shown  by  the  rock  (905)  of  the  large  outcrops  on  the  northwest  corner  of  the  island. 

The  Mosinee  hills  are  two  spurs  of  an  isolated  elevation  on  the  west  bank  of  the 
Wisconsin,  in  Sees.  27,  26,  25  and  22,  T.  28,  R.  7  E.,  Marathon  county.  They  are 
both  of  quartzite,  and  are  higher  than  the  rest  of  the  elevated  ground  around  them. 

The  Lower  Mosinee  hill  is  near  the  center  of  Sec.  27,  and  about  a  mile  from  the  river 
bank.  It  is  conical  in  shape,  with  slopes  of  about  30°  near  the  summit,  and  rises  to  an 
altitude  of  880  feet  above  Lake  Michigan,  or  about  280  feet  above  the  river  near  by. 
Its  slopes  and  summit  are  covered  with  loose  masses  of  quartzite,  one-foot  cube  to  four- 
feet  cube  in  size.  This  quartzite  (923)  or  quartz,  is  greyish-white,  occasionally  stained 
yellow,  vitreous,  and  translucent  in  thin  pieces,  and  peculiarly  brittle.  Sometimes  a 
slight  tendency  to  a  granular  structure  is  to  be  noticed. 

The  Upper  Mosinee  hill  is  reached  from  the  Lower  hill  by  crossing  a  saddle  between 
the  two.  On  this  saddle,  on  the  N.  E.  qr.  of  Sec.  27,  numerous  more  or  less  rounded 
fragments  of  a  fine-grained,  reddish  felspathic  rock  occur.  The  Upper  hill  is  on  the 
S.  E.  qr.  of  Sec.  23,  near  the  corner  of  the  section.  It  reaches  an  elevation  of  1,030 
feet,  or  about  430  feet  above  the  adjacent  river.  Its  slopes,  like  those  of  the  Lower  hill, 
are  covered  with  loose  angular  fragments  of  white,  vitreous  quartz  of  all  sizes,  up  to  five 


THE  ARCHAEAN  ROCKS. 


485 


feet  in  diameter.  On  the  summit  are  to  be  seen  some  large  irregular  exposures  of  the 
same  rock  (924),  showing  no  sign  of  bedding  structure.  None  of  the  quartzite  of  either 
hill  has  any  trace  of  lamination. 

About  three-quarters  of  a  mile  immediately  cast  of  the  Upper  hill,  at  the  water's 
edge  on  the  west  bank  of  the  Wisconsin,  is  a  low  outcrop,  several  hundred  feet  in 
length,  of  a  reddish  syenite.  At  the  upper  end  of  the  exposure  the  rock  (919)  is  very 
coarse,  composed  of  a  deep-red,  cleavable  felspar,  mottled  with  patches  of  brilliant 
black  hornblende,  up  to  a  quarter  of  an  inch  in  diameter,  and  showing  a  small  quantity 
of  translucent,  brownish-stained  quartz.  The  deep  red  color  is  evidently  partly  due  to 
weathering.  Two  sets  of  widely  separated  joints  occur,  one  set,  the  most  marked, 
bearing  N.  30°  E.,  the  other  N.  10°  W.  A  hundred  feet  below,  this  rock  changes  to  a, 
very  light-colored,  fine-grained  variety  (920),  poor  in  hornblende;  and  immediately  be- 
low again  to  a  very  coarse  kind  (921)  bluish-grey  in  color,  owing  to  the  preponderance 
of  large  surfaces  of  bluish,  cleavable,  non-striated  felspar,  and  mottled  with  black 
patches  of  hornblende.  This  is  evidently  the  normal  variety  from  which  the  reddish 
crumbling  kinds  result  by  weathering.  The  rock  of  this  exposure  is  the  same  that  is 


FIG.  15. 


QUARTZITE  EXPOSURE  ON  RIB  HILL,  MARATHON  COUNTY. 

largely  displayed  at  Big  Bull  falls,  five  miles  to  the  north,  and  is  entirely  unlike  any 
rock  noticed  farther  down  the  stream. 

Rib  hill,  on  Sees.  8  and  9,  T.  28,  R.  7  E.',  shows  large  exposures  of  the  same  sort 
of  quartzite  as  that  occurring  on  the  Mosinee  hills,  three  miles  southeast.  This  hill  is 
a  bold  isolated  crest,  about  a  mile  in  length,  trending  north  of  west,  across  the  southern 
half  of  Sec.  8,  and  gradually  increasing  in  height  from  an  altitude  of  1,143  feet  at  its 
eastern  extremity,  on  the  western  side  of  Sec.  9,  to  one  of  1,263  feet  at  its  western  ex- 
tremity near  the  west  line  of  Sec.  8.  This  western  end  is  thus,  so  far  as  definitely 
known,  the  highest  land  in  the  state.  It  rises  660  feet  above  the  Wisconsin  river,  three 
miles  east,  and  620  above  the  railroad  track  at  Wausau.  The  summit  of  the  hill  is 
rather  flat,  and  is  traversed  longitudinally  by  a  line  of  precipitous  exposures  of  quart- 
zite, from  five  to  forty  feet  in  height.  The  slopes  on  all  sides  are  very  steep  and  are 
covered  with  a  heavy  talus  of  loose,  angular  masses  of  quartzite,  of  all  sizes.  The 
northern  side  is  the  most  abrupt.  For  several  hundred  feet  it  slopes  away  from  the 
summit  at  angles  of  from  25°  to  30°. 

The  exposures  and  talus  show  everywhere  but  the  one  kind  of  rock  (927),  a  hard,  brit- 
tle, non-laminated,  glassy  translucent  quartz,  usually  of  a  dirty  white  color,  but  often 


486 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


FIG.  16. 


almost  colorless.  No  bedding  structure  was  observed,  the  rock  being  apparently  even 
Avithout  any  one  persistent  set  of  cross-joints,  though  all  of  the  exposures  show  frac- 
tures, some  quite  irregular,  and  others  approaching  to  plane  surfaces.  At  one  point 
several  parallel  N.  E.  joints  occur.  Fig.  15  is  a  sketch  of  one  of  the  large  exposures 
near  the  western  extremity  of  the  hill. 

On  the  Eau  Claire  river,  at  the  crossing  of  the  Stevens  Point  and  Wausau  road, 
Sec.  7,  T.  28,  R.  8  E.,  there  is  a  fall  over  coarse,  pinkish  syenite  (926)  resembling  that 
on  the  Wisconsin,  near  the  Mosinee  hills,  and  also  the  prevailing  syenite  at  Big  Bull 
falls,  a  short  distance  northward. 

On  the  upper  Eau  Claire,  in  Sec.  4,  T.  29,  R.  10  E.,  arg  exposures  of  a  very  coarse, 
rough-textured,  felspathic  granite,  consisting  of  pink,  cleavable  felspar;  very  large- 
flaked,  black  mica;  and  gray  quartz. 

At  AVatisau,  on  sections  25,  26,  35  and  36, 
T.  29,  R.  7  E.,  Marathon  county,  the  Wiscon- 
sin makes  bold  rapids  known  as  Big  Bull 
falls.  Here  the  river  is  divided  into  a  series 
of  channels  by  a  number  of  small  rocky 
islands,  and  the  exposures  are  large,  the  rock 
on  all  being  of  one  general  kind,  i.  e.,  syenite 
or  syenitic  granite.  This  syenite  varies  in 
degree  of  coarseness,  but  is  commonly  veiy 
coarse,  the  separate  minerals  being  very 
plainly  perceptible  to  the  naked  eye.  There 
is  no  resemblance  between  it  and  any  other 
rock  observed  on  the  Wisconsin  river,  except 
that  cf  the  Eau  Claire  river,  and  a  small 
outcrop  previously  alluded  to  as  near  the  up- 
per Mosinee  hill,  both  of  these  being  evi- 
dently merely  continuations  of  the  Wausau 
rock.  From  the  rock  of  Little  Bull  falls  it 
differs,  (1)  in  being  commonly  much  coarser 
in  grain,  (2)  in  having  usually  a  more  jagged 
fracture,  (3)  in  showing  greater  tendency  to 
iron-stain,  and  weather,  (4)  in  having  the 
hornblende  black  instead  of  greenish-black, 
(5)  in  having  the  felspar  orthoclase,  and  (6) 
in  containing  usually  some  blackish  mica. 

The  bedding  of  the  rocks  at  Big  Bull  is  for 
the  most  part  sufficiently  distinct,  the  general 
strike  being  N.  80°  E.  and  the  dip  from  30°  to 
40"  N.  W.,  most  commonly  about  38°.  In  a 
few  places  a  marked  gneissoid  structure,  co- 
inciding with  this  bedding,  and  owing  to  a 
parallel  arrangement  of  the  hornblende,  was 
observed.  For  the  most  part,  however,  the 
several  constituent  minerals  are  quite  uniformly  intermingled,  without  arrangement 
of  any  kind.  In  the  exposures  in  the  bed  of  the  stream,  and  on  the  walls  of  the  various 
channels,  large  bedding  -  plane  surfaces  frequently  show,  so  that  the  bedding  can  usually 
be  made  out  with  very  considerable  accuracy.  The  separate  layers  are  often  not 
more  than  2,  3,  or  4  inches  in  thickness. 

The  sketch  map,  Fig.  16,  serves  to  show  the  localities  of  the  various  exposures  exam- 
ined at  this  place.  Islands  No.  1,  2,  5,  8,  9,  10,  11  and  12  are  without  bare  rock.  The 


BIG       BULL       FALLS 


THE  AHCH^AN  EOCKS. 


main  or  west  channel  of  the  river,  between  island  No.  4  and  the  main-land,  shows  large 
exposures  both  in  the  bed  and  on  the  walls  of  the  gorge,  which  are  15  to  20  feet  in  height. 
A  section  in  this  channel  on  the  line  A  B,  bearing  N.  10°  W.,  and  beginning  a  short  dis- 
tance (100  feet)  above  the  bridge,  showed  the  following  succession,  the  measurements 

being  horizontal  distances : 

Feet. 

FIG.  17.  1.  Moderately  coarse  syenite  (912,  941):  brown- 
ish-pink to  gray,  mottled  with  black,  weath- 
ering with  a  dark-brown,  uniform-tinted 
surface.  Of  the  three  ingredients,  all  of 
which  are  very  plainly  perceived  by  the 
naked  eye,  the  felspar  is  much  the  coarsest, 
its  facets  reaching  %  inch  in  diameter;  in 
color  the  felspar  is  brownish-pink  to  gray, 
and  it  is  without  striations.  The  several 
ingredients  are  quite  uniformly  intermin- 
gled. In  most  of  this  measurement  the 
bedding  is  quite  distinct,  except  in  one  or 
two  places  where  it  is  obscured  by  cross- 
joints.  On  island  No.  3  prominent  joints 
trend  N.  78°  E.  and  dip  S.  E.  75°.  On  the 
•west  side  of  the  stream,  just  below  the 
\ragon  bridge,  the  bedding  planes  show 
finely  in  a  rock  somewhat  more  pink  than 
usual,  the  dip  being  38°  N.  W.  and  the 
strike  N.  80°  E.  The  same  rock  as  that  of 
this  measurement  shows  also  at  the  north 
end  of  island  No.  4,  and  on  the  small  rocky 
islet,  No.  6 490 

2.  Finer-grained  syenite  (907):   similar  to  the 

rock  of  No.  1,  but  of  grayer  color  from  the 
gray  color  of  the  felspar;  less  weathered 
and  of  a  finer  grain.  In  the  middle  of  the 
stream,  the  surface  of  the  layers  of  this 
rock  dip  very  plainly  30°  N.  "W.  Vertical 
joints  occur  here  nearly  along  the  strike. . .  116 

3.  Still  finer-grained  syenite  (908) :   dark  gray 

to  black  in  color;  much  more  hornblendic 
and  less  quartzose  than  the  preceding  kinds. 
The  junction  of  this  rock  with  No.  2  is  quite  sharp,  and  shows  well  on  the 
east  side  of  the  gorge,  where  the  bedding  is  also  quite  plainly  to  be  seen, 
with  a  strike  of  N.  75°  E.,  and  a  dip  of  38°  N.  W.  Prominent  cross- 
joints  occur  at  this  place,  trending  with  the  strike  direction,  and  standing 
vertically 202 

4.  No  exposures 62 

5.  Coarse  syenite  (911):   allied  to  the  rock  of  No.  1  (912,  907),  but  containing 

much  more  pink  orthoclase;  penetrated  by  many  patches  and  veins  of  a  fine- 
grained, but  distinctly  crystalline,  dark-gray  to  black,  hornblendic  rock.  A 
large  one  of  these  veins  is  represented  by  Fig.  17 165 

6.  No  exposure 70 

7.  Very  coarse  syenite  (910j:  bluish-gray,  showing  large  unstriated  grayish  fel- 

spar surfaces,  and  coarse  brilliant  black  hornblende,  in  pieces  up  to  %  inch 


BLACK  VEIN  IN  S  YE  NITS, 
WAUSAU. 


488  GEOLOGY  OF  CENTRAL  WISCONSIN. 

by  }£  inch;  containing  but  little  quartz.     The  weathered  crust  of  this  rock    Feet. 
is  y^  inch  thick,  dark-brown  outside,  and  pure  white  beneath,  the  latter  due 

evidently  to  kaolinization 125 

8.  Coarse  iron-stained  syenite  (909) :  close  to  the  preceding,  but  not  quite  so 
coarse,  and  having  the  felspar  brownish  from,  iron-staining,  and  more 
abundant 80 


Total  horizontal  length  of  section 1 ,230 

Thickness  of  rock  layers  about 600 


On  Island  No.  7  of  Fig.  19,  are  exposures  which  lie  south  of  the  end  of  tlois  section. 
At  the  north  end  of  the  island,  the  rock  (941)  resembles  No.  1  of  the  section,  and  con- 
tains a  vein  of  reddish  telepathic  granite  30  feet  long,  1  foot  wide,  and  having  a  central 
band  of  white  quartz.  1  inch  to  2  inches  wide.  At  the  south  end  of  the  island  a  long, 
low  exposure  shows  a  fine-grained,  light-pinkish,  distinctly  gneissoid  syenite,  or  syenitic 
granite  (943),  which  is  very  much  more  quartzose  than  any  of  the  other  Wausau  rocks. 
The  quartz  is  granular,  glassy  and  wine-colored.  The  parallel  grain  is  due  to  an  ar- 
rangement of  the  black  hornblende,  which  stands  out  quite  prominently  against  the 
surrounding  light-colored  quartz. 

At  the  point  C  of  Fig.  19,  on  the  west  side  of  the  river,  and  near  the  north  line  of  Sec. 
26,  a  large  exposure  shows  rocks  quite  different  from  those  at  the  falls  below.  The 
main  rock  (915)  at  this  place  is  fine-grained,  dark-gray  and  hornblendic,  having  a  dis- 
tinctly parallel  structure,  and  weathering  to  a  light-pinkish  color.  A  number  of  heavy 
beds  of  this  rock  are  to  be  seen  dipping  20°  to  26°  N.  W.,  and  striking  N.  60°  E.,  thus 
corresponding  in  bedding  with  the  rocks  at  the  falls.  Intersecting  the  dark-colored  rock 
are  numerous  small  pinkish  veins.  In  one  place,  on  the  river  edge,  a  large,  smooth 
joint-surface  shows  a  nearly  horizontal  vein  16  inches  wide,  the  vein  matter  (916)  being 
composed  of  pink  cleavable  felspar  and  limpid  white  quartz.  Cutting  vertically  through 
this  vein  and  the  inclosing  rock  is  a  mass  of  a  very  fine-grained,  decomposing,  schistose 
chloritic  rock  (917),  4  feet  wide,  having  its  lamination  vertical.  The  lines  of  demarka- 
tion  between  the  three  kinds  of  rock  on  this  exposure  are  all  very  sharply  defined. 

On  the  Jenny  road,  on  the  east  side  of  the  Wisconsin,  N.  hf.  Sec.  24,  T.  29,  R.  7  E., 
1%  miles  from  Wausau,  are  several  low  outcrops  of  a  white- weathering,  in  places  iron- 
stained,  slaty  quartzite  (931).  On  a  fresh  fracture  this  rock  presents  a  non-crystalline, 
whitish  aspect,  and  is  quite  hard.  With  a  lens,  a  few  minute  felspar  fiacets  are  seen. 
Fynte  is  present  in  minute  cubes.  Some  specimens  show  a  slight  tendency  to  effervesce 
in  hot  acid.  The  schistose  structure  is  evident,  the  planes  striking  N.  85°  E.,  and  dip- 
ping 50°  N.  W. 

One  and  a  half  miles  further  north,  the  same  road  ascends  Marshall  hill.  All  along 
this  hillside  in  sections  12  and  1  are  large,  angular  fragments  of  a  fine-grained,  gray- 
ish, aphanitic,  silicious- schist  (930).  This  rock  is  quite  soft,  very  distinctly  laminated, 
splitting  very  readily  across  the  lamination  planes.  Some  specimens  effervesce  very 
slightly  on  heating. 

Eastward  from  Wausau,  on  the  north  line  of  T.  29,  R.  8  E.,  the  country  rises  rap- 
idly, and  is  traversed  by  numerous  low  but  abrupt  ridges,  such  as  are  characteristic  of 
large  portions  of  the  Archaean  area.  No  rock  outcrops  were  noted  on  any  of  these,  but 
angular  fragments  of  a  white-weathering,  porphyritic  rock  (929)  were  seen  in  great 
abundance.  This  rock  has  an  aphanitic,  light  grey,  not  very  hard  matrix,  through 
which  arc  scattered  a  few  felspar  facets,  and  numerous  amygdules  of  translucent, 
brownish  quartz,  the  latter  reaching  %  inch  in  diameter.  It  was  noticed  most  abund- 
antly on  Sec.  33,  T.  29,  R.  7  E. 

Westward  from  Wausau,  in  T.  29,  R.  7  E.,  a  number  of  outcrops  occur.  Near  its 
south  line,  this  town  is  traversed  by  Rib  river.  In  Sees.  21,  22,  27  and  28,  there  is 


THE  ARCILEAN  ROCKS. 


489 


high  ground  trending  north  and  south,  which  rises  200  to  300  feet  above  the  Wisconsin 
at  Wausau.  In  the  S.  E.  qr.  of  Sec.  21,  on  the  south  slope  of  part  of  this  ridge,  a 
peculiar,  fine-grained  felspathic  rock  (937,  945)  is  exposed,  and  is  quarried  to  some  ex- 
tent on  Mr.  Kolter's  land.  This  rock  has  a  brownish-pink  color,  the  least  weathered 
portions  showing  a  grayish  tinge,  is  rather  fine-grained,  and  has 'a  marked  granular 
texture,  looking  almost  like  a  mechanical  rock.  The  most  abundant  ingredient  is  a 
pinkish  felspar  in  cleavable  fragments  up  to  ^\ih  inch  across.  With  this  is  much 
granular  brownish  quartz,  and  a  little  blackish  mica  in  fine  flakes,  making  the  rock  a 
granite.  No  arrangement  of  the  minerals  in  parallel  lines  is  perceptible.  In  the  quarry 
the  rock  is  seen  to  be  nearly  horizontal,  dipping  not  more  than  10°  in  a  due  south  direc- 
tion. A  total  thickness  of  about  three  feet  was  seen.  Large  thin  slabs,  2  inches  to  4 
inches  thick,  splitting  off'  parallel  to  the  bedding,  can  be  obtained. 

Nea,r  Single's  Mill,  in  the  north  part  of  S.  E.  qr.  of  Sec.  29,  in  the  same  township, 
and  on  the  edge  of  a  part  of  the  same  high  ground,  are  exposures  of  a  whitish,  slaty, 
granular  quartzite  (936),  in  places  iron-stained.  Under  the  magnifying  glass  this  rock 
is  seen  to  be  made  up  of  rounded  grains  of  glassy  quartz.  Some  few  places  were  noted 
where  the  variety  with  granular  texture  grades  into  a  non- granular  glassy  quartz. 
Scales  of  silvery  mica  occur  on  the  surfaces  of  laminae.  The  bedding  structure  is  distinct, 
and  shows  a  strike  of  N.  75°  E.  and  dip  of  56°  S.  E. 

About  half  a  mile  from  this  place,  and  on  the  south  side  of  the  valley  of  Little  Rib 
river,  S.  E.  qr.  Sec.  29,  the  northeast  face  of  a  ridge  shows  quartzite  in  large  exposures. 
The  rock  here  (935)  is  glassy,  translucent,  and  occasionally  iron-stained,  resembling  that 
of  Rib  Hill.  The  bedding  is  obscure.  On  the  slope  of  the  hill  below,  the  roots  of  the 
trees  of  a  heavy  wind-fall  have  upturned  numerous  fragments  of  a  brownish-pink,  gran- 
ular-textured felspathic  rock,  similar  to  that  at  Kolter's  quarry  in  Sec.  21.  Half  a  mile 
northeast  on  the  north  face  of  the  same  elevation,  N.  E.  qr.  S.  E.  qr.  Sec.  30,  a  high 
ledge  shows  the  same  felspathic  rock,  striking  N.  80°  E.,  and  dipping  50°  N.  W. 

At  the  falls  of  Rib  river,  S.  E.  qr.  Sec.  28,  T.  29,  R.  5  E.,  are  large  exposures  of 
greenish  chloritic  schist  and  syenite.    On  the  south  side  of  the  river,  at  a  point  near  the 
lower  left  hand  comer  of  Fig.  18,  is  a  rocky  point  about  15  feet  high,  showing  heavily 
but  distinctly  bedded,  greenish  syenite,  dipping  20°  E.,  and  striking  N.  8°  W.     The  up- 
permost layer  (950),  3  feet  thick,  is 

FIG.  18.  moderately  coarse-grained,   mottled 

green  and  grey,  weathering  white. 
To  the  lens  it  shows  much  grayish 
quartz,  green  amphibole,  and  white 
altered  felspar,  the  last  least  abund- 
ant, though  coarsest  of  the  three.  In 
some  specimens  greenish  chlorite  ac- 
companies the  hornblende.  The  next 
layer  below  (948),  4  feet  thick,  is  a 
very  much  finer  -  grained,  almost 
aphanitic,  greenish-grey  rock,  cou- 
containing  apparently  a  good  deal  of 
chlorite.  The  weathered  surface  is 
white,  with  numerous  green,  epidotc- 
colored  blotches.  Microscopic  exam- 
ination shows  that  the  ingredients  of 
this  fine-grained  rock  are  the  same 
as  those  of  the  coarser  one  above,  but 
that  the  amphibole  and  felspar  arc 
both  more  altered.  This  rock  breaks 


tfectitrn  cm  the  line  B.C.J^E. 

BOTK  OCCUKHBNCHS  AT  THE  FALLS  OF  RlB  RtVDK. 

Scale,  fifty  feet  to  the  inch. 


490  GEOLOGY  OF  CENTRAL  WISCONSIN. 

out  very  readily  into  rectangular  blocks,  the  planes  of  easiest  cleavage  lying  at  right 
angles  to  the  bedding.  The  lowest  layer,  3  feet  thick,  is  again  of  a  coarse  (949)  variety 
like  that  of  the  uppennost  bed. 

On  the  north  side  of  the  river,  beginning  from  the  point  B,  we  find  a  continuous  low 
exposure,  extending  several  rods  up  the  stream,  and  showing  the  same  bedding  structure 
as  seen  on  the  south  side  of  the  river.  Passing  over  these  exposures  on  the  line  B  C, 
at  right  angles  to  the  strike,  we  find  first,  for  40  feet,  mottled,  grayish  syenite  (951), 
resembling  that  on  the  south  side  of  the  river,  but  somewhat  finer  in  grain.  The 
weathered  surface  "is  of  a  uniform  green  hue,  and  a  cross-fracture  shows  a  greenish 
chloritic  crust  extending  inward  as  much  as  j^  inch,  with  a  sharply  defined  inner  edge. 
Beyond  on  the  line  B.  C.  is  first  seen  a  similar  rock,  which  is  however,  more  highly 
quartzose  and  felspathic,  the  amphibole  being  almost  excluded  (952).  Beyond  again  green 
chlorite  begins  to  appeal-,  gradually  increasing  in  quantity,  the  former  dip  and  strike 
joints  at  the  same  time  becoming  confused  by  the  introduction  of  schistose  planes,  until, 
at  80  feet  from  the  beginning,  the  rock  has  become  a  well-marked  green  chloritic  schist, 
the  schistose  planes  bearing  N.  45°  E.,  and  dipping  60°  to  80°  S.  E.  The  gradation  of 
the  one  rock  into  the  other  is  unmistakable.  Beyond  again  the  chlorite-schist  is  largely 
exposed,  and  extends  entirely  across  the  river,  forming  the  barrier  rock  of  the  falls.  Its 
most  common  variety  (953)  is  dark  green  in  color,  with  large,  interlocking,  greasy-sur- 
faced laminae.  The  schistose  surfaces  are  readily  scratched  with  a  knife,  but  much  sili- 
cious  matter  is  present.  Pyrite  is  also  to  be  seen  throughout.  In  places  the  im- 
purity is  less  than  usual,  and  the  rock  nearly  all  chloritic  (954).  After  crossing  about 
25  feet  of  this  schist,  its  lamination  lines  are  seen  to  become  again  obscure,  signs  of  the 
former  low  dip  reappearing,  and  the  rock  becoming  again  l.ke  that  below  (955). 

We  seem  to  have  in  these  rocks  an  instance  of  the  change  of  an  amphibolic  to  a 
chloritic  rock,  with  a  simultaneous  production  of  schistose  planes  crossing  the  ordinary 
bedding  lines. 

At  Marathon  City,  Sec.  6,  T.  28,  R.  6  E.,  a  low  exposure  occurs  on  the  edge  of  the 
water  in  Rib  river,  which  shows  syenite  (957)  closely  allied  to  the  coarser  syenite  at  Rib 
river  falls.  It  is  medium-grained,  dark-greenish  and  grayish,  showing  surfaces  of  bril- 
liant black  lamellar  hornblende  up  to  ^  inch  in  diameter,  embedded  in  a  matrix  of  very 
fine-granular  quartz,  and  coarser,  white,  glassy  felspar.  The  hornblende  facets  fre- 
quently show  a  tendency  to  alteration,  and  are  then  ill-defined  on  the  edges,  from  the 
surrounding  matrix. 

The  rocks  of  Rib  river  falls  and  Marathon  City  bear  a  resemblance  to  those  found 
crossing  the  Wisconsin  at  Mosinee,  but  are  rather  more  chloritic,  or  altered.  The  strike 
directions  at  the  two  places,  N.  5e  to  10"  W.  at  Mosinee,  and  N.  8°  W.  at  Rib  river 
falls,  also  correspond.  It  seems  probable  that  the  two  are  portions  of  a  continuous  belt 
trending  west  of  north.  If  so,  the  belt  must  have  a  considerable  width,  for  the  strike 
direction  at  Mosinee,  if  carried  out  northward,  would  not  reach  so  far  west  as  the  falls 
of  Rib  river. 

YELLOW  RIVER  VALLEY. 

The  upper  part  of  Yellow  river,  in  Wood  county,  north  of  the  Green  Bay  and  Minne- 
sota Railroad,  flows  over  gneissic  and  granitic  rocks,  which  are  exposed  nearly  continu- 
ously in  the  beds  and  on  the  sides  of  the  stream,  for  many  miles.  The  same  is  true  of 
the  branches  of  the  river  in  this  part  of  its  course. 

On  the  divide  between  Yellow  and  Black  rivers,  sandstone  extends  far  to  the  north- 
ward, covering,  and  for  the  most  part  concealing,  the  crystalline  rocks,  which,  however, 
occasionally  rise  through  the  sandstone.  The  boundary  between  the  formations  it  is 
almost  impossible  to  trace  accurately,  since  the  irregular  surface  of  the  crystalline  rocks 


THE  ARCILEAN  ROCKS.  ,        49! 

beneath  may  bring  them  up  through  to  the  surface  at  any  point.  The  same  is  true  to 
some  extent  of  the  region  between  Yellow  river  and  the  Wisconsin,  but  here  the  sand- 
stone does  not  extend  nearly  so  far  north. 

In  Hemlock  Creek,  at  the  crossing  of  the  wagon  road  from  Grand  Rapids  to  Dexter- 
ville,  N.  E.  qr.  of  the  S.  E.  qr.  of  Sec.  5,  T.  22,  R.  4  E.,  are  ledges  of  rather  fine-grained, 
flesh-colored,  gneissoid  granite  (967).  Translucent,  wine-colored  quartz,  and  pinkish 
orthoclase  in  small,  brilliant  facets,  make  up  most  of  the  rock;  the  mica  is  sparse,  in 
fine,  green-black  flakes,  which  have  a  distinct  linear  arrangement.  This  rock  is  a  hand- 
some one,  and  would  probably  dress  well,  though  showing  some  tendency  to  weather 
and  iron-stain.  The  bedding  directions  appear  to  show  a  strike  of  N.  60*  E.,  and  a  dip 
of  70°  S.  E. 

On  Yellow  river  itself,  the  southernmost  Archaean  exposure  is  to  be  seen  about  two 
miles  north  of  Dexterville,  in  the  N.  hf .  of  Sec.  14,  T.  22,  R.  3  E.  The  rock  here  is 
medium-grained,  pinkish,  quartzosc,  gneissoid  granite  (973),  composed  chiefly  of  limpid 
quartz  and  orthoclase  felspar,  the  former  the  most  abundant.  Mica  is  present  in  fine 
black  scales  arranged  in  parallel  lines.  The  strike  appears  to  N.  55°  W.,  and  the  dip 
60°  S.  W.  Near  the  top  of  the  river  bank,  which  rises  directly  from  the  granite,  thin- 
bedded,  friable,  horizontal  sandstone  is  exposed. 

On  Sec.  3,  T.  22,  R.  3  E.,  three  miles  north  of  Dexterville,  there  are  large  flat 
ledges  in  the  bed  of  the  river,  of  gneiss,  bounded  on  the  north  by  quartz-porphyry.  The 
gneiss  (969  and  971)  is  very  fine-grained,  laminated,  dark  gray  to  black  in  color,  and 
consists  of  a  black  mineral  (mica,  hornblende,  or  both),  in  small  brilliant  flakes;  and 
whitish  quartz  and  felspar.  Its  weathered  surface  is  earthy  and  of  a  dirty  white  color, 
but  shows  the  fine  lamination  even  more  distinctly  than  the  interior.  The  quartz- 
porphyry  (970)  consists  of  a  light  greenish-grey,  aphanitic  matrix,  having  the  peculiar 
flaky  appearance  that  is  characteristic  of  the  quartz-porphyries  of  the  various  isolated 
Archaean  patches  of  Wisconsin,  in  which  are  imbedded  somewhat  sparsely  scattered 
facets  of  pinkish  orthoclase  felspar  up  to  one  sixteenth  of  an  inch  in  diameter.  It  is  a 
very  tough,  compact,  rock;  and  is  worn  by  the  running  water  into  smoothed  and 
polished  surfaces.  This  porphyry  appears  to  penetrate  the  adjacent  laminated  rock  in  a 
very  irregular  manner.  In  one  place  amass  of  the  gneissoid  rock,  some  50  feet  in  di- 
ameter, is  nearly  surrounded  by  the  porphyry,  the  lines  of  junction  between  the  two  be- 
ing very  sharp,  and  rendered  especially  noticeable  by  the  different  appearances  of  their 
weathered  surfaces.  The  lines  of  junction  are  not  curved,  but  straight,  bearing,  re- 
spectively, N.  70°  W.,  N.  30°  E.,  and  N.  70°  W.;  the  first  and  last  on  opposite  sides  of 
the  enclosed  mass.  The  strike  of  the  gneiss  is  N.  25°  W.,  its  dip  60°  N.  E.  The 
porphyry  is  20  to  30  paces  wide,  and  appears  to  be  bounded  on  the  north  by  the  same 
gneiss  as  before,  with  the  same  bedding.  Beyond,  porphyry  again  comes  in. 

At  Pitts'  Mill,  five  miles  north  of  Dexterville,  on  Sec.  34,  T.  23,  R.  3  E.,  are  very  large 
exposures  on  Yellow  river,  which  passes  here  through  a  narrow  rocky  gorge,  of  a  very 
beautifully  and  coarsely  banded  gneiss  (993),  the  bands  being  alternately  dark-gray  to 
black,  and  bright  pink,  and  having  a  northwest  direction.  The  dark-colored  bands 
predominate,  and  run  from  %  inch  to  one  or  two  feet  in  breadth,  but  when  so  broad,  are 
rarely  free  from  fine  h'nes  resembling  the  material  of  the  pink  bands,  which  run  in 
width  from  these»fine  lines  up  to  6  or  10  inches.  The  dark-colored  portions  are  fine- 
grained, with  an  intimate  parallel  structure,  and  consist  predominatingly  of  fine  green- 
ish-black mica,  with  which  are  seen  fine  white  and  red  felspar  facets,  and  some  fine 
quartz.  In  places,  greenish  black,  cleavable  hornblende  appears  to  partly  replace  the 
mica.  The  red  bands  consist  chiefly  of  coarse-grajned  orthocla&e  felspar,  with  some 
limpid  granular  quartz  and  occasional  blotches  of  mica,  and  show  numerous  whitish 
kaolinized  patches,  the  whole  rock  having  a  tendency  to  decompose.  Several  folds  in 
the  strata  occur,  and  are  rendered  especially  striking  by  the  very  marked  red  and  black 


492  GEOLOaY  OF  CENTRAL  WISCONSIN. 

banding.  A  complete  arch  is  to  be  seen  on  the  east  bank  of  the  river  in  front  of  Mr. 
Pitts'  house.  The  plane  of  the  bank,  which  at  this  point  is  about  15  feet  in  height,  cuts 
directly  across  the  strike,  and  slopes  towards  the  northwest  at  an  angle  of  45°.  Its  base 
joins  another  surface  sloping  about  10°  in  the  same  direction.  Along  both  surfaces  the 
individual  layers  can  be  traced  until  they  meet  near  the  top  of  the  bank.  The  central 
part  of  the  fold  as  seen  on  both  surfaces  is  a  confused  and  largely  kaolinized  felspathic 
mass  (994). 

On  the  N.  E.  qr.  Sec.  21,  T.  23,  R.  3  E.,  Rocky  Run  enters  Yellow  river,  which  hero 
traverses  for  many  rods  a  rocky  gorge,  below  which  exposures  continue  along  the  river 
for  a  long  distance.  About  half  a  mile  below  the  mouth  of  Rocky  Run,  gneiss  is  ex- 
posed, striking  N.  W.  and  dipping  E.,  and  traversed  by  a  vein  3  feet  wide  of  a  fine- 
grained, black,  hornblendic  rock.  The  vein  cuts  diagonally  the  lamination  lines  of  the 
gneiss.  Beginning  about  twenty  rods  below  the  mouth  of 'Rocky  Run,  and  extending 
up  to  it,  are  ledges  of  a  fine-grained,  greenish-grey,  micaceous  granite  (974),  which  con- 
sists of  very  fine  greenish-black  mica,  predominating,  translucent  quartz  and  pink  or- 
thoclase.  In  places  occurs  a  more  highly  felspathic,  reddish  kind  (975),  which  appears 
sometimes  to  enclose  portions  of  the  darker  colored  variety.  No  definite  bedding  struc- 
ture was  observed.  Traversing  this  granite  are  numerous  thin  veins  %  to  %  inch 
in  width,  of  white  quartz,  pink,  cleavable  orthoclase,  and  greenish  epidote.  The  felspar 
veins  are  in  places  so  numerous  as  to  make  up  a  large  portion  of  the  rock.  The  epidote 
veins  fault  the  others,  being  apparently  the  most  recent.  Fig.  19  represents  a  face  3 

feet  by  1%  feet.     Nearly  all  of  this  rock 

1 10.  19.  shows  a  decided  tendency  to  weather,  be- 

ing in  places  altered  to  an  impure  kaolin. 
Kaolin  is  reported  to  occur  in  quantity  at 
points  in  the  vicinity.  From  the  crumb- 
ling condition  of  the  rocks,  this  would  seem 
very  probable. 

Five  miles  north  of  Pitt's  Mill,  in 
the  northern  part  of  Sec.  3,  T.  23,  R.  3  E., 
the  bed  of  Yellow  river  is  made  for  15 
rods  of  a  coarse-grained,  flesh-colored  gran- 
FAULTED  VEINS  IN  GRANITE,  YELLOW  RIVEK.      ite'  consisting  of  a  very  uniform  admixture 

of  flesh-colored  orthoclase,  glassy  quartz, 
and  black  mica.     No  distinct  bedding  is  to  be  seen. 

At  Big  Bull  Falls,  nine  miles  north  of  Pitt's  Mill,  on  Sec.  15  and  16,  T.  24,  R.  3  E., 
large  exposures  of  medium-grained,  highly  felspathic,  red  granite  extend  along  the 
bed  and  in  the  banks  of  Yellow  river  for  a  quarter  of  a  mile.  This  granite  has  a  base 
of  cleavable  reddish  orthoclase,  throughout  which  is  quite  uniformly  distributed  hyaline, 
occasionally  smoky,  quartz,  in  irregularly  shaped  patches  ^2d  to  ^th  inch  in  diameter. 
Mica  is  present,  but  is  very  fine  and  sparse.  For  the  whole  length  of  the  exposure,  this 
rock  is  nearly  uniform,  and  without  any  tendency  to  kaolinize.  Its  peculiar  texture, 
composition  and  color  combine  to  make  it  a  very  valuable  and  unusually  handsome 
building  granite.  Polished  specimens  of  the  rock  attracted  great  attention  at  the  Phila- 
delphia Exposition,  where  it  was  regarded  by  experts  as  among  the  finest  of  the  many 
polished  granites  exhibited. 

On  Sec.  7,  T.  24,  R.  3  E.,  another  exposure  of  a  similar  red  granite  was  noted.  Above 
this  point,  Yellow  river  is  reported  without  exposures. 


PLATE,XVII 


FORMATIO  X  «  a  lo  ,irf  13  LAC  K  R 

///  .Ircti oii.i  2,1l,i4,faa/itf22, 
Town  21  Rautfe 
•  JACKSON    CO. 

•  )><•/  /r.fm  •"  '• 


Lower  Siluriu  i 


Gi'auite  ItornblemlpMaafiLeHiauFerru&uTious         Polsdjuli 
Rot-k  Si-liisl      (>iiartzS<-lii.s+       Sandstone- 


THE  ARCELEAN  ROCKS. 


493 


BLACK  RIVER  YALLEY. 

The  first  exposures  of  crystalline  rocks  met  with  in  ascending  Black  river  are  found  a 
short  distance  below  the  town  of  Black  River  Falls,  T.  21,  R.  4  W.,  in  Jackson  county. 
From  here  they  occur  in  the  bed  and  on  the  sides  of  the  stream,  with  only  occasional  inter- 
ruptions, as  far  north  as  town  28,  in  Clark  county.  For  the  greater  part  of  this  distance, 
they  are  concealed,  away  from  the  river,  by  overlying  horizontal  sandstone,  through 
which,  however,  they  occasionally  rise  in  knobby  projections.  In  some  of  the  branch 
streams,  also,  the  sandstone  is  cut  through  and  the  crystalline  rocks  exposed.  Along 
the  river  the  rock  ledges,  in  few  places  only,  rise  to  any  considerable  height  above  the 
water. 

In  the  vicinity  of  Black  River  Falls  the  exposures  are  large  and  interesting.  The 
map  of  Plate  XVII  shows  the  relative  positions  of  the  various  outcropping  beds,  their  bed- 
ding and  dip  directions  being  shown  by  the  accompanying  section.  From  these  it  will 
lie  seen  that  at  this  place  a  central,  nearly  structureless,  granitic  mass  is  bounded  on  the 
southwest  by  layers  of  gneiss,  dipping  southwestward,  into  which  it  appears  to  grade; 
and  on  the  northeast,  by  a  succession  of  scliistose  beds,  dipping  northeastward,  but  not  hav- 
ing exactly  the  same  strike  directions  as  the  gneiss  on  the  other  side.  In  the  following 
detailed  descriptions,  the  various  rock  masses  are  numbered  as  on  the  map  and  section, 
beginning  with  the  gneiss  on  the  southwest: 

FIG.  20. 


UNCOHFORMABILITT,  BLACK  RIYER  FALLS. 

I.  Gniess  (1,015):  rather  fine-grained,  very  plainly  laminated,  pink  and  gray 
banded;  dipping  S.  W.  60°,  striking  N.  32°  W.  The  constituent  minerals 
are:  pinkish  orthoclase,  predominating;  pinkish  and  colorless  translucent 
quartz;  mica  in  very  fine  black  scales,  but  quite  abundant,  and  much  more 
plenty  in  certain  layers  than  in  others;  and  also  a  whitish,  partly  altered, 
felspar,  in  fine  facets.  In  some  places,  especially  micaceous  portions  have 
a  much  darker  color  than  usual;  in  others  large  nests  of  coarse,  cleavable 


GEOLOGY  OF  CENTRAL  WISCONSIN. 

pink  orthoclase  occur.  The  laminae  are  for  the  most  part  not  over 
l-32d  inch  in  width,  remarkably  regular  and  parallel,  and  without 
contortion.  Two  sets  of  veins  traverse  the  rock,  both  of  reddish  felspar, 
those  of  one  set  being  but  mere  strings  and  faulting  the  others,  which  are 
one-fourth  to  one-half  inch  in  width.  This  gneiss  is  exposed  for  several 
hundred  feet  along  the  river  opposite  Ledyard's  old  mill;  and,  as  shown  on 
the  map  and  section,  is,  at  the  lower  end  of  the  exposure,  overlaid  by  25  to 
30  feet  or  more  of  horizontal  sandstone,  which  fills  in  the  depression  in  the 
very  irregular  upper  surface  of  the  gneiss.  The  exact  junction  of  the  two 
formations  is  distinctly  to  be  seen  for  a  long  distance.  In  some  places  the 
gneiss  shows  no  alteration  at  its  contact  with  the  sandstone;  in  others 
again,  as  it  is  traced  upward  from  the  water's  edge  to  the  line  of  contact, 
a  rapidly  increasing  decomposition  is  observed,  until  immediately  below 
the  sandstone  the  change  to  a  soft  bluish-white  clay  or  kaolin  (1,018)  is 
complete.  The  kaolin  retains  still  very  plainly  the  fine  lamination  of  the 
unaltered  gneiss,  it  being  even  possible  in  some  cases  to  trace  individual 
laminae  from  the  unchanged  into  the  kaolinized  rock.  Immediately  below 
the  sandstone  the  laminae  of  the  softened  rock  are  seen  to  be  bent  over  as 
though  by  the  weight  of  the  superincumbent  sandstone.  This  is  a  fact  of 
some  interest,  since  it  would  confirm  the  view  already  presented,  that  the 
kaolinization  was  subsequent  to  the  deposition  of  the  sandstone;  having 
been  caused  possibly  by  the  currents  of  carbonated  water  which  found  pas- 
sage along  the  junction  line  of  the  two  formations.  A  section  through  the 
sandstone,  kaolin,  and  gneiss,  is  presented  in  Fig.  20.  Up  the  river 
gneiss  continues  to  show,  losing,  gradually,  its  distinct  lamination,  to  with- 
in a  short  distance  of  the  wagon  bridge,  above  which,  after  an  interval 
without  exposures,  granite  appears. 

la.  Granite  (1,008):  medium-grained,  pinkish,  consisting  of  a  nearly  uniform 
admixture  of  pinkish  orthoclase,  in  facets  up  to  l-16th  inch,  and  fine- 
grained translucent  quartz.  Some  mica  is  present,  in  fine  scales,  showing 
sometimes  a  slightly  stringy  arrangement.  This  granite  is  exposed  from  a 
short  distance  above  the  wagon  bridge,  as  far  north  as  the  north  line  of 
Sec.  14,  the  river  in  this  distance  passing  through  a  gorge  whose  walls 
sometimes  reach  a  height  of  80  feet.  In  the  large  exposures  at  the  falls, 
the  parallel  grain  of  the  gneiss  below  is  almost  entirely  lost,  being  only 
occasionally  indicated  in  an  obscure  arrangement  of  the  mica.  The  rock 
here  is  traversed  by  several  sets  of  joints  mostly  somewhat  irregular,  those 
showing  the  greatest  irregularity  trending  N.  80°  E.  and  dipping  72°  S.  E. 
but  having  no  corresponding  structure  in  the  rock.  Above,  the  granite 
shows  the  same  general  characters  as  at  the  falls,  occasionally  —  as  in  the 
railroad  cut  on  the  west  side  of  the  river,  just  above  the  falls  —  showing  a 
darker  kind  than  usual  from  a  greater  quantity  of  fine  dark  mica.  In  this 
cut  there  are  to  be  seen  two  sets  of  planes  equally  marked,  one  set  trend- 
ing N.  W.  and  dipping  N.  E.,  the  other  trending  N.  E.  and  dipping  N. 
W.  A  distinct  stringy  arrangement  of  the  mica  was  noted  parallel  to  the 
former  set.  Near  the  north  line  of  Sec.  15,  the  granite  exposures  cease 
suddenly  on  the  east  side  of  the  river,  whilst  they  continue  some  distance 
farther  on  the  west  side  —  a  fact  to  be  explained  by  the  northwest  strike  of 
the  succeeding  slaty  rocks. 

II.  Hornblende  rock  or  schist  (501):  fine-grained,  crystalline-textured;  dark- 
colored  to  black;  breaking  with  conchoidal  fracture;  weathering  out;  into 
rough  prismatic  fragments,  with  dirty  brown  color;  striking,  as  a  whole, 


THE  ARCILEAN  ROCKS.  495 

N.  "W.    This  rock  is  exposed  in  a  low  lodge  on  the  east  side  of  the  river,     Feet. 
almost  immediately  succeeding  the  granite.      It  shows  also,  on  a  small 
rock  in  the  middle  of  the  stream,  where  a  distinct  contorted  lamination  is 

observable.     Horizontal  width 60 

III.  Magnesian  slate  (516,  522) :  pale-gray,  light-greenish-grey,  dark-green,  oc- 
casionally pink,  or  even  bright  brick-red,  from  presence  of  iron  sesquioxide; 
sometimes  quite  soft,  at  others  quite  hard  and  gritty,  from  the  presence  of 
fine  granular  quartz,  which  appears  never  to  be  entirely  absent;  highly 
schistose,  the  laminae  striking  N.  60°  W.  and  dipping  N.  E.  70C.  The 
magnesian  mineral  appears  to  be  talc  in  the  light-green  kinds,  and  chlo- 
rite in  the  dark  green,  the  former  kind  much  predominating,  and  never- 
sharply  defined  from  the  other.  The  light-gray  to  nearly  whitish  kinds  are 
the  most  silicious,  and  most  firm,  the  others  showing  much  tendency  to 
crumble  and  decompose.  Tins  is  especially  so  with  those  that  are  stained 
bright-red,  their  contained  oxide  of  iron  arising  from  the  oxidation  of  py- 
rite,  which  sometimes  is  to  be  seen  still  unchanged,  in  minute  cubes.  These 
schists  are  exposed  on  the  east  side  of  the  river,  on  a  nearly  perpendicular 
bank,  100  feet  in  height,  which  forms  the  western  end  of  "Tilden's  Iron 
Mound."  About  75  feet  along  the  river  bank  from  the  lower  end  of  the 
exposure,  a  bright-red  layer,  30  feet  thick,  occurs,  in  which  hematite  forms 
a  prominent  constituent,  the  surfaces  of  some  of  the  laminse  having  even  a 
bright  specular  lustre  (522)  and  in  which  nests  and  seams  of  porous,  iron- 
stained  quartz  are  quite  abundant.  At  one  time  this  ferruginous  schist 
was  mined  as  an  iron  ore.  Averaged  specimens  from  it  yielded  respectively 
9.81.  28.13  and  31. 27  per  cent,  of  metallic  iron;  the  first  representing  a  thick- 
ness of  24  feet,  near  the  water's  edge,  the  second  the  same  thickness  at  an 
elevation  of  30  feet  above  the  river,  the  third,  6  feet,  more  ferruginous 
than  the  rest,  immediately  next  below  (stratigraphically)  the  preceding 
layer.  The  six  feet  layer  does  not  continue  the  whole  height  of  the  bank. 
The  length  of  the  exposure  of  this  rock  along  the  river  bank  is  about  700 

feet,  its  horizontal  width  about 200 

l\    Covered:  on  Tilden's  Iron  Mound 550 

V.  Ferruginous  quartz- schist:  finely  laminated,  varying  from  a  light  gray, 
somewhat  ferruginous  quartz-schist,  to  a  dark-colored  highly  magnetic 
rock;  in  many  places  weathered  brownish,  iron-stained,  partly  crumbling. 
Tins  rock  is  exposed  in  a  low  outcrop  on  the  water's  edge  on  the  east  bank 
of  the  river;  in  a  similar  low  outcrop  on  the  west  bank;  and  again  (appar- 
ently the  same  layer)  some  distance  east  from  the  river  on  the  north  flank 
of  the  Iron  Mound,  at  points  indicated  on  the  map.  The  first  exposure 
shows  a  very  much  decomposed,  crumbly,  brown-stained,  non-magnetic 
rock,  containing  42.32  per  cent,  of  metallic  iron.  The  outcrop  on  the  west 
bank  of  the  river  is  somewhat  larger,  showing  a  material  similar  to  that 
on  the  east  side,  with  a  very  plain  N.  50°  W.  strike,  and  N.'  E.  dip.  A 
sample  across  the  whole  width  of  30  feet  yielded  35.96  per  cent,  of  iron. 
The  exposures  on  the  Iron  Mound  are  partly  artificial,  a  considerable  quan- 
tity of  the  rock  having  been  removed  for  smelting  purposes.  In  one  of  the 
two  main  openings  the  rock  or  ore  is  brown-stained  and  magnetic,  contain- 
ing 34.22  per  cent,  of  metallic  iron;  in  the  other,  somewhat  deeper  in  the 
hill,  a  much  less  oxidized  material  is  seen.  Of  this,  the  innermost  portions 
present  a  dark-gray  to  nearly  black  appearance,  and  exceedingly  fine- 
grained texture,  being  composed  of  alternating  darker  and  lighter  colored  % 
(more  quartzose)  bands,  but  having  this  banding  much  less  prominent  than 


496  .      GEOLOGY  OF  CENTRAL  WISCONSIN. 

on  the  weathered  kinds.    This  dark-colored  rock  is  distinctly  magnetic,     feet. 
affecting  the  needle,  and  adhering  to  a  magnet  in  quite  coarse  particles. 
An  averaged  sample  yielded  32.1  per  cent,  of  iron.     A  partial  analysis  of 
the  same  material  yielded  the  writer,  in  1872,  the  following  results: 

Per  cents. 

Metallic  iron 31 .87 

Silica 45.72 

Lime 1 .62 

Alumina 8.56 

Magnesia •  •  •  •  trace. 

Still  another  sample,  averaged  from  the  whole  opening,  and  from  the 
stock  pile  outside,  yielded  37.18  per  cent,  of  metallic  iron.  The  horizontal 
width  of  this  schist  seen  on  the  river  is 60 

VI.  Magnesian  schist:  similar  to  No.  Ill;  bedding  very  plain;  strike  N.  50°  W., 

dip  60°  N.  E. ;  width 20 

VII.  Covered.    In  this  interval  the  west  side  of  the  river  begins  to  rise,  the  cnst 

side  being  now  depressed  into  the  valley  of  Levins'  creek.  On  each  side  of 
the  mouth  of  this  creek,  and  extending  up  it  for  a  long  distance,  are -ledges 
of  thin-bedded,  horizontal  sandstone,  which  thus  overlies  and  conceals  the 
Archaean  rocks,  filling  the  depressions  in  their  ancient  eroded  surface. 
The  Archsean  exposures  are  now  transferred  to  the  west  side  of  the  river. 
The  horizontal  width  of  this  gap  at  right  angles  to  the  general  strike,  is . .  100 

VIII.  Magnesian  schist:   light-colored;   silicious;  similar  to  No.  VI;   showing 
plainly  the  same  bedding  structure;  width 40 

IX.  Ferruginous  quartz- schist  (513):  fine-grained,  dark-gray,  very  quartzose; 

showing  under  the  lens  numerous  grains  of  glassy,  quartz,  which  occur 
more  abundantly  on  some  seams  than  others.  Seams  and  surfaces  stained 
red;  non-magnetic;  contains.  26.98  per  cent,  metallic  iron;  strike  N.  45° 
W.;  width 24 

X.  Magnesian  schist  (511,512):  in  the  lower  or  more  southern  portions  quite  soft 

(512);  light  greenish-gray,  and  without  indication  of  any  quartzose  ingre- 
dient; towards  the  upper  portions  becoming  much  more  quartzose  (511), 
losing  the  softness  and  greenish  tinge.  In  these  last,  the  lens  reveals 
much  granular,  glassy,  translucent  and  smoky  quartz  between  the  laminae; 
width 200 

XI.  Covered 120 

XII.  Magnesian  schist  (504):  greenish  gray;  having  thin  intercalated  bands  of 

ferruginous  quartz-schist;  width 120 

XIII.  Ferruginous  quartz- schist:  very  much  weathered.     An  old  pit  has  been 
sunk  on  this  near  the  water's  edge.    The  loose  material  in  the  pit  yielded 
30.23  per  cent,  metallic  iron.    The  width  seen  is 60 

Nos.  XII  and  XIII  are  well  exposed  in  the  railroad  cutting  at  the  top  of 
the  bank,  about  80  feet  high,  at  whose  foot  the  pit  alluded  to  is  sunk.  The 
cutting  is  not  quite  in  the  line  of  strike,  being  nearly  north  and  south.  In 
it  are  exposed,  beginning  at  the  north  end  (a)  magnesian  schist  (508),  6 
feet  horizontal  width;  (b)  banded  ferruginous  quartz  schist,  containing 
29.17  per  cent,  of  metallic  iron,  2  feet;  (c)  magnesian  schist  with  thin 
seams  of  ferruginous  quartz-schist,  13  feet;  (d)  ferruginous  quartz- schist, 
with  small  seams  of  magnesian  schist  —  the  more  ferruginous  portions  con- 
taining 26.04  per  cent,  of  iron —16  feet;  (e)  the  same  as  the  last,  but  con- 
taining more  magnesian  bands,  grading  into  the  next  layer,  16  feet;  (f) 
ferruginous  schist,  with  many  magnesian  bands,  cut  into  small  prismatic 


THE  ARCII^IAN  ROCKS.  497 

blocks  by  close  jointing  and  containing  28.63  per  cent,  of  Iron,  48  feet.     Feet. 
Returning  now  to  the  river  bank  below,  we  note  next; 

XIV.  Magnesian  schist:  (502,  503)    60 

XV.  Covered:  by  sandstone.     Immediately  north  of  the  magnesian  schist  No. 

XIV,  and  resting  cb'rectly  against  it,  horizontal  sandstone  is  seen  and  con- 
tinues to  show  in  mural  exposures  10  to  40  feet  in  height,  all  along  the 
west  bank  of  the  river  to  a  point  beyond  the  limits  of  the  section  The 
width  of  the  gap  is  about 3,500 

XVI.  Ferruginous  quartz-schist:  much  oxidized,  containing  32.91  per  cent,  of 

iron 8 

XVII.  Mica  slate:  finely  laminated;  very  light- colored;  the  mica  in  bright-lus- 
tered  plates  up  to  %  inch  in  diameter 5 

XVIII.  Ferruginous    quartz-schist  (1017):    fine-grained,   veiy  thinly  and  dis- 
tinctly laminated,  without  contortion;  brownish  to  grayish  black  in  color; 
non-magnetic;   streak  red;    under  the  lens  seen  to  consist  of  mingled 
grains  of  white  quartz,  and  a  metallic-lustered  black  mineral  (hematite  ?) ; 
contains  iron,  32.49  per  cent 32 

XIX.  Covered 22 

XX.  Ferruginous  quartz-schist:  resembling  No.  XVIII  7 

Nos.  XVI,  XVII,  XVIII,  and  XX,  all  show  plainly  a  strike  of  N.  65° 
W.,  and  dip  of  70°  N.  E.  With  the  exception  of  XVIII,  which  rises 
10  feet  from  the  river,  they  are  all  seen  on  very  low  exposures  barely  ris- 
ing from  the  water,  and  overlaid  by  heavy  beds  of  sandstone,  which  shows 
in  a  perpendicular  face  in  the  bank  above.  The  exact  junction  of  No. 
XVIII  with  the  overlying  sandstone  is  well  exposed,  it  being  possible  to 
obtain  hand  specimens  showing  both  formations  (1009).  One  of  these 
has  already  been  figured  on  page  462.  Another  remarkable  feature  in 
these  exposures  is  the  bending  of  the  sandstone  layers  above,  to  conform 
with  the  irregular  surface  of  the  schistose  rocks,  suggesting  the  idea  that 
a  motion  upward  of  the  schist  had  caused  the  bending,  which  is  seen,  not 
only  in  the  lower  layers,  but  also  in  the  heavy  ones  6  to  10  feet  above. 
This  feature  is  represented  in  Fig.  21. 

At  the  junction  of  the  two  rocks,  the  sand  is  seen  to  have  frequently  been 
wedged  between  the  partly  separated  schist  laminae,  and  in  one  place  in- 
cludes a  detached  mass  of  the  schist. 

XXI.  Covered  by  sandstone , 150 

XXII.  Ferruginous  quartz-schist 3 

XXIII.  Covered 40 

XXIV.  Ferruginous  quartz-schist  (519) 5 

Total  horizontal  width  of  the  slaty  series  measured 5,406 

Approximate  thickness 5, 000 


Nos.  XXII  and  XXI V  occur  on  the  east  bank  of  the  river,  and  are  barely 
seen  above  the  water's  edge,  being  overlaid  by  heavy  beds  of  sandstone. 

The  existence,  in  the  region  about  Black  River  Falls,  of  isolated  hills  of  ferruginous 
schist,  which  rise  through  the  surrounding  horizontal  sandstone,  has  already  been  alluded 
to.  These  hills  are  known  locally  as  "iron  ore  mounds."  They  are  from  100  to  250 
feet  in  height,  and  rise  somewhat  abruptly  from  the  level  sandy  plain,  which  is  also 
dotted  by  loftier  castellated  outliers  composed  of  higher  layers  of  the  same  sandstone  as 
that  which  forms  its  basement.  The  rocks  of  the  "  iron  ore  mounds  "  strictly  come  un- 
der another  head,  being  isolated  areas  of  Archaean;  but  are  conveniently  alluded  to  here 
Wis.  SUK.— 32. 


498 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


on  account  of  their  close  relations  to,  and  short  distance  from,  the  slaty  rocks  just  de- 
scribed as  occuning  on  Black  river.  For  the  positions  of  the  various  mounds,  see  Atlas 
Plate  XV,  Area  F.  The  exposures  observed  on  them  are  mostly  poor,  and  nearly  always 
of  ferruginous  quartz-schist,  like  that  occurring  on  Black  river,  and  quartz.  On  those 
mounds,  however,  which  lie  on  sections  15  and  14,  T.  21,  R.  3  W.,  and  Sec.  31,  T.  22, 
R.  3  W.,  the  iron  oxide,  instead  of  being  magnetic,  or  red,  or  brown  and  hydrated,  is 
brilliant  specular  hematite.  The  specimens  from  the  mound  on  Sec.  12,  T.  21,  R.  4  W., 
show  chiefly  a  dark-colored  magnetic  rock,  like  that  of  Tilden's  iron  mound.  On  the 
mound  on  Sec.  17,  T.  21,  R.  3  W.,  white  quartz  only  was  observed. 

The  considerable  amount  of  iron  in  the  schists  of  Black  river,  and  of  the  mounds  in 
the  neighboring  country,  has  for  many  years  attracted  attention  to  these  rocks,  it  being 
supposed  that  they  were  of  value  as  ores  of  iron.  Several  attempts  at  smelting  have  been 
made.  One  small  furnace  was  built  on  the  banks  of  Levin's  creek,  as  long  ago  as  1855, 
and  another  begun,  but  never  completed,  on  the  south  side  of  Tilden's  mound,  near  the 
river.  In  the  first-named,  the  ferruginous  quartz-schist  of  the  north  side  of  Tilden's 
monnd  was  mixed  with  the  hematitic  magnesian  schists  from  the  west  side  of  the  same 
mound  on  the  river  bank.  As  a  flux  for  this  mixture,  a  dolomitic  limestone  from  the  Lower 
Magnesian  formation  was  used.  It  may  be  readily  seen  that  no  successful  work  was 
ever  done. 

In  view  of  the  considerable  interest  that  had  been  excited  with  regard  to  these  ores, 
and  the  reputation  they  had  already  attained,  the  writer  was  sent,  during  the  first  year 

Fig.  21. 


B 


ID 


POTSDAM  SANDSTONE  ON  ARCHAEAN  SCHISTS. 

XVI  Ferruginous  quartz-schist,  8  feet.  XVII  M;ca  Schist,  6  feet.  XVIII  Ferruginous  schist, 
23  feet.  XX  Ferruginous  schist,  7  feet.  A,  mass  of  Schist  included  in  the  sandstone.  BB,  Pots- 
dam sandstone,  top  layers  feet  thick.  Scale,  31)  feet  to  1  inch.  C.  D.,  River  level. 


of  the  present  survey,  by  the  then  Chief  Geologist,  Dr.  I.  A.  Lapham,  to  make  an  exam- 
ination as  to  their  value.  Samples  for  analysis  were  averaged  from  all  the  exposures 
and  in  all  the  openings  seen;  and  analyses  made  of  most  of  the  samples,  especially  with 
regard  to  their  richness  in  iron.  The  ores  or  iron-bearing  rocks  are  of  two  general 
lands:  the  ferruginous  quartz-schists,  in  which  the  iron-bearing  ingredient  is  at  different 
times  magnetite,  specular  hematite,  red  hematite,  and  the  brown  or  hydrated  oxide  — 
the  last  two  probably  from  weathering  only  —  and  the  ferruginous  magnesian  schists, 
in  which  the  iron  oxide  is  red  hematite.  Of  the  former  kind,  the  various  samples  yielded 
respectively,  26.04,  26.98,  28.63,  29.17,  30.23,  30.90,  31.87,  32.10,  32.49,  32.91,  34.22, 
35.96,  37.18  and  42.52  per  cents,  of  metallic  iron.  Of  the  latter,  observed  only  in  one 
place,  the  samples  yielded  9.81,  28.13  and  31.27  per  cents.1  In  the  first  kind,  the  only 
other  important  ingredient  besides  iron  oxide  is  quartz;  in  the  second,  a  silicate  of  mag- 

i  For  the  "hard"  or  silicious  ores  of  Michigan,  50  per  cent,  of  iron  is  the  minimum  amount  at 
which  the  ores  can  find  purchasers. 


THE  ARCHAEAN  ROCKS. 


499 


nesia.  Though  obtained  on  carefully  selected  samples,  the  above  figures  are  probably 
somewhat  high.  Whilst  iron  ores  are  worked  with  even  lower  percentages  than  these, 
such  admixtures  as  quartz  and  magnesian  silicates  would  necessitate  quantities  of  iron 
at  least  half  as  large  again.  The  Black  river  "  ores  "  then,  really  cannot  be  regarded  as 
ores,  but  are  properly  iron- bearing  rocks.  Whether  valuable  working  ores  may  yet  be 
discovered  in  these  slaty  rocks  is  another  question.  Similar  rocks  occur  with  the  work- 
able ores  of  Michigan.  Taking,  however,  all  the  circumstances  into  account,  it  is  deemed 
rather  improbable  that  such  ores  can  exist.  Even  if  they  do,  they  are  not  likely  to  be 
discovered,  but  rather  to  remain  hidden  underneath  the  sandstone  that  forms  the  surface 
rock  throughout  the  region. 

It  has  been  said  on  a  previous  page  that  the  peculiar  lithological  characters  of  the 
slaty  rocks  of  Black  river,  and  of  the  mounds  of  the  vicinity,  strongly  suggest  their 
Huronian  age  —  a  suggestion  which  is  partly  corroborated  by  their  position  on  the  border 
of  the  great  Archaean  area  of  the  north  part  of  the  state.  It  has  been  supposed  that 
the  granite  and  gneiss  of  the  foregoing  section  were  Laurentian,  the  slaty  rocks  Huro- 
nian. From  the  details  given  it  will  be  seen  that  all  must  be  assigned  to  the  same 
series. 

At  Black  River  Station,  on  Sec.  3,  T.  22,  R.  3  W.,  where  the  Green  Bay  and  Min- 
nesota Railway  crosses  Black  river,  crystalline  rocks  are  exposed  in  the  side  and  bottom 
of  the  gorge  through  which  the  river  passes,  and  are  overlaid  at  the  top  of  the  banks  by 
a  few  thin  layers  of  sandstone.  The  river  here  trends  about  S.  25°  W.,  or  in  a  direc- 
tion roughly  at  right  angles  to  the  general  strike.  The  southernmost  exposure  examined 
was  about  a  quarter  of  a  mile  below  the  railroad  bridge.  Beginning  with  it,  and  pass- 
ing northward  on  the  west  bank  of  the  river,  the  following  different  rocks  were  noticed : 

FIG.  22. 


CONTORTED  GNEISS  ON  BLACK  EIVER. 

I.  Gneiss:  showing  in  a  rounded  knob  some  25  feet  above  the  water,  and  about  100  feet 
long,  and  in  the  river  bed  below  for  about  200  feet  northward.  At  the  southern 
end  of  the  exposure  the  gneiss  (1,000)  is  very  fine-grained,  thinly  laminated,  pink- 
ish-weathered, and  quartzose;  consisting  of  fine-granular,  glassy  quartz,  predom- 
inating; fine  pinkish  felspar,  and  fine  black  mica,  arranged  in  lines,  the  lamina- 
tion of  the  rock  being  also  independent  of  the  arrangement  of  the  mica;  having 
a  strike  of  N.  35°  W.,  and  a  dip  of  62°  N.  E.  A  hundred  feet  northward  this 
merges  into  a  kind  (1,001)  in  which  the  granular  quartz  still  more  largely  predom- 
inates, and  the  mica  is  almost  wholly  absent.  A  short  distance  beyond,  this  changes 
again  to  a  dark  colored,  beautifully  contorted  kind  (1,002),  consisting  of  fine-grained 


500  GEOLOGY    OF   CENTRAL  WISCONSIN. 

white  quartz,  partly  arranged  in  separate  white  bands,  up  to  one  inch  in  width, 
and  partly  also  mingled  with  fine,  brilliant  black  mica,  and  fine,  white  felspar,  in 
dark  gray  bands.  The  weathered  surface  of  this  is  dark  brown  with  a  white  kao- 
linized  undercrust.  North  of  the  gneiss  no  rock  occurs  for  400  feet,  then  come 
outcrops  some  500  feet  long  of, 

It.  Diorite  (1,003):  rather  coarse-grained,  highly  crystalline,  grayish,  felspathic;  com- 
posed of  large  surfaced,  bluish-gray  felspar,  with  coarse  hornblende;  without  def- 
inite bedding  structure.  Underneath  the  railroad  bridge  this  rock  is  terminated 
by  a  mass  or  vein  of, 

IIL  White  quartz:  5  feet  wide.  Immediately  next  to  which  begin  .outcrops  about  200 
feet  long  of 

IV.  Gneiss  (1,005  and  1,006):  rather  fine-grained,  pink- and- gray-banded,  very  quartz- 

ose;  consisting  principally  of  pink  and  colorless  translucent  quartz,  with  some  fine 
greenish-black  mica  and  pinkish  orthoclase;  in  places  a  quartzite  (1,004),  the  oth- 
er minerals  being  almost  wholly  absent.  Above  this  the  rocks  are  concealed  for  a 
short  distance,  after  which  are  seen,  some  20  feet  in  width,  of 

V.  Micaceous  schist  (1,007);  a  very  peculiar,  fine-grained,  dark-brown,  earthy-textured, 

jointed  rock.  Under  the  lens  it  is  seen  to  consist  largely  of  angular  grains  of 
quartz.  The  smooth  jointed  planes  of  this  rock  strike  N.  W.,  and  stand  vertical. 

In  the  river  one  mile  above  Rlack  River  Station,  a  ledge  150  feet  long  and  25  feet 
high,  is  seen,  of  fine-grained,  dark-reddish  granite  (990),  consisting  of  a  rather  uniform 
and  close  admixture  of  reddish  orthoclase,  in  fine  glittering  facets,  reddish-brown,  trans- 
lucent quartz,  some  colorless  quartz,  and  a  little,  sparsely  scattered,  fine  black  mica. 
Half  a  mile  further  up  stream,  fine-grained,  red  and  gray  banded,  quartzose  gneiss 
(991)  is  exposed.  The  gray  bands  consist  of  fine-grained,  glassy  quartz,  fine  black  mica 
and  white  felspar;  the  red  of  brown  and  red  translucent  quartz,  mingled  with  a  little 
orthoclase.  From  here  to  the  mouth  of  the  East  Fork,  the  bed  of  Black  river  shows  nu- 
merous small  ledges,  3  to  4  feet  high,  of  contorted  gneiss  and  reddish  granite. 

Above  the  mouth  of  the  East  Fork,  which  is  on  Sec.  36,  T.  23,  R.  3  W.,  exposures 
of  red  granite  are  seen  as  far  as  French's  mill,  on  Sec.  25.  The  wagon  road  which, 
for  half  a  mile  below  the  mill,  follows  the  west  bank  of  the  river  has,  on  the  east  side, 
ledges  of  red  granite,  and  on  the  west,  a  ridge  thirty  to  forty  feet  high,  composed  of 
horizontal,  coarse-grained,  quartzose,  cross-laminated  sandstone.  In  one  place,  the 
exact  junction  of  the  two  formations  is  to  be  seen.  At  the  mill,  the  granite  exposures 
are  especially  large,  both  on  the  west  bank  and  on  a  large  island  in  the  stream.  Two 
kinds  of  the  granite  occur,  both  presenting  a  prevailing  pinkish  weathering:  (1)  a  rather 
fine-grained,  very  uniform- textured,  dark  reddish  kind  (988,  close  to  990);  and  (2),  a 
medium-grained,  uniform-textured,  pinkish-grey,  quartzose  kind  (987),  containing 
both  colorless  glassy,  and  pink  translucent  quartz;  pink  orthoclase;  and  fine  black 
brilliant  mica.  Both  kinds  appear  like  handsome  building  or  ornamental  granites.  No 
definite  bedding  structure  is  to  be  seen. 

On  the  wagon  road,  three  quarters  of  a  mile  south  of  Neillsville,  Sec.  22,  T.  24,  R. 
2  W.,  is  a  large  outcrop  200  yards  long,  and  10  to  40  feet  high,  of  porphyritic,  cal- 
careous gneiss,  striking  E.  W.,  and  dipping  80°  S.  At  the  northern  end  of  the  ex- 
posure, the  rock  (984),  is  medium-grained,  fine-laminated,  knotty,  and  highly  mica- 
ceous. Fresh  surfaces  show  a  large  quantity  of  fine-flaked  brilliant  black  mica,  white 
quartz  in  little  nests,  around  which  the  micaceous  laminae  curve,  and  white  felspar, 
which  sometimes  occurs  in  smaller  nests  up  to  a  quarter  to  half  inch  in  diameter.  In 
large  quantity,  the  pulverized  rock  effervesces  briskly  in  muriatic  acid.  In  the  middle 
portion  of  the  ledge,  the  rock  (985),  closely  resembles  that  just  described;  but  shows 
much  pink  cleavable  felspar  and  less  mica,  the  pink  felspar  forming  the  knots.  At  the 


PLATE.XVm 


.•i/iftifiiif/  Ilit'  relative  position* 
f,ftJn- 

i  s  o  i. ,VT  K  u   A  u  r  H  AK  AN    A  R  K  A  w 

fdl  i.*<-<»i.<tin    < 
R.  D.  Irviiia 


A  H   AT  IT  O/N 


()uartz  Porphyry  UIUIIIII  GraTiite 


THE  ARCHAEAN  ROCKS.  501 

routh  end,  the  gneiss  resembles  that  at  the  northern  end,  and  contains  large  masses  of 
\vhite  quartz,  up  to  ten  by  four  feet  in  size. 

These  .knotty  gneisses  resemble  closely  others  which  occur  on  the  line  of  the  Wiscon- 
sin Valley  Railroad,  in  Portage  county. 

Three-quarters  of  a  mile  west  of  Neillsville,  at  the  crossing  of  Black  river,  on  the  S. 
W.  qr.  Sec.  15,  T.  24,  R.  2  W.,  fine-grained,  light- pinkish,  slightly  gneissoid,  and  very 
quartzose  granite  (983)  is  exposed,  with  a  vertical  dip  and  E.  W.  strike.  This  rock  is 
very  hard  and  compact,  and  appeal's  to  be  a  fine  ornamental  granite. 

Tne  gneissoid  and  red  granites  of  Black  and  Yellow  rivers  resemble  one  another 
dosely,  and  appear  to  be  directly  continuous  with  one  another  underneath  the  sandstone, 
which  nearly  everywhere  between  the  two  rivers  is  the  surface  rock.  Occasionally  the 
crystalline  rocks  come  to  the  surface  in  the  interval,  and  are  then  of  the  same  character 
as  on  the  rivers;  as  for  instance,  on  0'NeiTs  creek,  in  Sees.  1  and  2,  T.  24  R.  1  W., 
Clark  county,  where  red  granite  is  exposed;  and  on  a  high  bluff  in  the  N.  E.  part  of  T. 
23.  R.  2  E.,  whose  upper  portions  are  reported  to  be  of  red  granite  with  sandstone  layers 
at  lower  levels. 

The  amount  of  these  reddish  ornamental  granites  of  extraordinarily  fine  quality  occur- 
ring on  Yellow  and  Black  rivers,  and  in  the  intervening  country,  appears  to  be  very- 
great. 

THE  ISOLATED  AROLEAN  AREAS. 

I.  In  General. 

We  have  next  to  consider  those  isolated  areas  of  Archaean  rocks 
which  are  found  protruding  through  the  surrounding  horizontal  Silu- 
rian strata,  at  points  widely  scattered  over  the  central  part  of  the 
state.  Plate  XVIII  is  a  sketch  map  showing  the  relative  positions 
of  these  various  areas,  as  also  the  nature  of  the  rocks  of  each  area, 
and  its  distance  from  the  southern  boundary  of  the  main  Archaean 
mass. .  Near  to  this  boundary  line  it  is  not  always  possible  to  be  sure 
that  we  have  to  deal  with  an  isolated  area,  when  we  find  a  mound-like 
exposure  of  crystalline  rocks,  with  sandstone  showing  in  the  vicinity 
at  lower  levels,  on  account  of  the  intricate  and  somewhat  indefinite 
nature  of  the  boundary  itself.  Besides  these  doubtful  areas,  which 
may  be  somewhere  connected  with  the  main  Archaean  region  without 
intervening  horizontal  strata,  there  are,  however,  many  others  which 
occur  as  much  as  50  or  100  miles  within  the  region  of  the  Lower  Si- 
lurian rocks.  Underneath  these,  the  connection  with  the  rocks  of  the 
main  Archaean  area  is,  of  course,  preserved,  the  separation  being  su- 
perficial only.  All  of  the  scattered  patches  are  but  points  of  the  uni- 
versal Archaean  basement,  upon  which  all -the  later  strata  are  built, 
having  earned  their  especial  immunity  from  complete  burial  by  virtuo 
of  the  resistant  nature  of  their  materials.  They  are  properly  buried 
mountains,  and  were  high  islands  and  reef-ledges  in  the  early  Paleozoic 
yeas. 


502  GEOLOGY  OF  CENTRAL  WISCONSIN. 

All  the  areas,  except  the  one,  or  rather  the  group,  including  the 
Baraboo  ranges  in  Sank  county,  are  of  small  size,  generally  occupying 
much  less  than  a  square  mile  of  area.  With  the  same  exception,  they 
are  all  mound-like  in  form,  rising,  usually,  somewhat  abruptly  from 
the  surrounding  country,  which  is  frequently  level,  and  showing  al- 
ways considerable  rock  exposures  on  the  flanks  and  summits,  being 
often  almost  all  of  bare  rock.  They  reach  heights  of  from  50  to  250 
feet,  but  are  usually  lower  than  surrounding  outlying  bluffs  of  the 
horizontal  strata.  The  Baraboo  group,  unlike  the  others,  constitutes 
a  series  of  bold  ridges,  one  of  which  reaches  elevations  of  800  and  900 
feet  above  Lake  Michigan,  and  a  length  of  over  20  miles.  These 
ranges  are  so  important  an  element  in  the  topographical  features  of 
Central  Wisconsin,  that  they  have  already  received  attention  in  the 
chapter  on  general  topography.  They  are  still  more  fully  described 
in  subsequent  pages. 

The  nature  of  the  rocks  composing  the  several  areas  is  not  always 
the  same.  The  large  areas  in  Sauk  county,  and  a  few  others,  are 
chiefly  of  quartzite;  a  number  are  of  quartz-porphyry;  still  others 
of  granite,  which  is  different  in  different  cases;  and  yet  others,  occur- 
ing  in  Jackson  county,  and  close  to  the  main  Archaean  area,  are  of 
ferruginous  quartz-schist. 

Except  in  the  cases  of  the  granitic  areas,  these  rocks  arc  generally 
quite  distinctly  bedded,  and  are  usually  tilted  at  high  angles. 

In  many  of  the  areas,  especially  in  those  whose  elevation  is  consid- 
erable, horizontal  sandstone  is  found  lying  immediately  against  the 
tilted  crystalline  rocks,  pebbles  and  boulders  from  which  frequently 
occur  in  the  sandstone,  giving  it  often  a  rough,  conglomeratic  charac- 
ter, and  proving  at  once  the  great  antiquity  and  non-intrusive  nature 
of  the  rocks  from  which  they  are  derived.  Some  of  the  areas  have, 
without  doubt,  been  once  entirely  buried  beneath  the  sandstone  layers, 
to  whose  subsequent  denudation  they  owe  their  resurrection. 

The  following  tabulation  gives,  in  a  condensed  manner,  and  in  a 
form  convenient  for  comparison,  the  location,  size,  nature,  etc.,  of  each 
of  the  known  areas.  The  facts  with  regard  to  Nos.  II,  III,  XI,  XIII 
and  XVIII,  are  furnished  by  Prof.  Chamberlin,  in  whose  report  de- 
scriptions of  them  will  be  found. 


THE  ARCHAEAN  ROCKS. 


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oiH  GEOLOGY  OF  CENTRAL  WISCONSIN. 

II.  Special  Descriptions  of  the  Several  Areas. 
THE  BAKABOO  QUARTZITE  KANGES. 

The  Baraboo  quarfczite  ranges  occupy  much  the  largest  extent  of  territory,  and  are 
at  the  same  time  much  the  most  striking  and  most  important  as  influencing  the  to- 
pography of  the  state,  of  any  of  the  isolated  Archaean  areas  that  occur  within  the  region 
of  the  Silurian  rocks.  Their  bold  character,  and  the  dissimilarity  between  their  rocks 
and  those  of  the  country  around,  have  drawn  to  them  the  attention  of  previous  State 
Geologists,  as  weh1  as  of  other  scientific  men.  Percival1  regarded  the  quartzitcs  com- 
posing the  ranges  as  resulting  from  a  metamorphism  of  the  Potsdam  sandstone  of  the 
surrounding  region.  Hall2  refers  them  correctly  to  the  Archaean,  making  them  Huro- 
rian,  but  his  detailed  examinations  were  not  published.  Alexander  Winchell3  calls  them 
"Lower  Potsdam,"  on  the  evidence  of  some  fossils  belonging  to  the  middle  Potsdam, 
and  found  in  the  sandstone  lying  against  the  quartzite.  This  he  regards  as  proving  the 
"  Lower  Potsdam  "  age  of  the  quartzite,  losing  sight  of  the  fact  that  the  latter  is  uncon- 
formable  with  the  sandstone,  and  projects  upwards  into  the  horizon,  not  only  of  the 
middle  Potsdam,  but  even  far  above  into  that  of  the  St.  Peters.  The  Archaean  age  of 
the  quartzite  was  first  definitely  proved  by  the  writer  in  1872,4  and  this  conclusion  has 
since  been  abundantly  confirmed  by  the  work  of  other  geologists,5  and  also  by  his  own 
further  researches  in  the  region. 

The  Baraboo  Bluffs  constitute  two  east  and  west  ranges  extending  some  25  miles  in 
length  through  the  towns  of  Caledonia,  in  Columbia  county,  and  Greenfield,  Merrimack, 
Sumpter,  Baraboo,  Honey  Creek,  Freedom,  Excelsior  and  Westfield,  in  Sank  county. 
The  southern  one  of  the  ranges  is  much  the  bolder  and  more  continuous,  and  the  two 
are  not  exactly  parallel,  but  diverge  as  they  are  traced  westward.  At  their  eastern  ends, 
in  Columbia  county,  they  unite  in  a  bold  point,  rising  abruptly  from  the  low  ground  of 
the  Wisconsin  river,  here  at  the  easternmost  point  of  the  great  bend  which  the  quartzite 
ranges  compel  it  to  take.  Tracing  them  westward,  we  find  the  two  ridges,  about  mid- 
way in  their  lengths,  some  four  miles  apart,  and  at  their  western  ends  a  mile  or  so  more 
than  this;  Here  a  bold,  nearly  north  and  south,  cross-ridge,  also  with  a  quartzite  core, 
unites  the  two,  thus  finishing  an  entire  cordon  of  bluffs  around  a  depressed  interior.  All 
around  the  outside  of  this  circuit  of  hills,  except  beyond  the  western  cross-ridge,  the 
country  is  comparatively  low,  and  often  quite  level,  so  that  the  ridges  rise  very  boldly, 
forming,  for  a  non-mountainous  country,  quite  a  striking  feature  of  the  landscape. 

The  southern  quartzite  range  is  broken  down  in  only  one  place,  the  gorge  in  which 
lies  the  Devil's  Lake,  and,  as  seen  from  the  low  ground  of  the  Wisconsin  river  on  the 
south,  presents  a  continuous,  wavy  crest,  often  with  large  areas  of  bare  rock,  and  with 
elevations  of  from  -500  to  700  feet  above  the  river,  and  of  700  to  900  feet  above  Lake 
Michigan.  Its  higher  portions  have  a  width  of  from  one  to  four  miles,  the  outline  being 
quite  irregular  on  account  of  the  deep  and  very  anciently  eroded  valleys  that  indent  its 
sides.  The  great  antiquity  of  these  vaUeys  is  evinced  by  their  showing  on  their  sides 
and  bottoms  layers  of  horizontal  sandstone  clinging  to  the  underlying  quartzite.  The 
sandstone  has  evidently  been  deposited  in  valleys  which  were  originally  formed  long 
before  its  deposition,  and  have  been  carved  out  anew  in  the  same  places,  on  account  of 

i  "Annual  Report  of  the  Geological  Survey  of  Wisconsin,"  1836,  p,  101. 

»  Geology  of  Wisconsin,  1862. 

8American  Journal  of  Science  II,  vol.  xxxvii,  p.  226. 

4  Am.  Journal  of  Science,  Feb.,  1872. 

*  See  J.  H.  Eaton  "  On  the  .Relations  of  the  Sandstones,  Conglomerate  and  Limestone,  of  Sank 
county  to  each  other  and  to  the  Azoic,"  Am.  J.  Sci.  Ill,  vol.  V,  p.  144,  and  T.  C.  Chamberlin  on  the 
"  Methods  of  Upheaval  of  the  Baraboo  Ranges,"  Wis.  Acad.  Sci..  vol.  IT. 


THE  ARCHAEAN  ROCKS.  505 

its  friable  and  non-resistant  nature.  The  country  on  top  of  the  range  is  heavily  timbered 
presenting  in  this  regard,  as  also  in  its  almost  universal  heavy  clay  soil,  a  marked  con- 
trast with  the  lower  country  around.  This  clay  soil  has  caused  the  making  of  many  ex- 
cellent farms  on  top  of  the  range.  It  occurs  alike  on  the  quartzite  and  the  high-level 
sandstone.  In  the  eastern  extension  of  the  bluffs  it  might  be  regarded  as  of  glacial  ori- 
gin, but  to  the  westward  the  glacial  drift  limit  is  reached  about  midway  in  the  length 
of  the  range,  and  some  other  origin  must  be  sought. 

The  northern  range  is  much  less  pronounced  than  the  southern.  For  about  seven 
miles  west  from  the  junction  of  the  two,  in  Columbia  county,  it  f orms  a  continuous  ridge 
some  300  to  400  feet  in  height,  but  generally  much  less  than  a  mile  in  width.  Further 
west  its  height  lessens  for  long  distances,  the  Archaean  rocks  forming  its  core  at  -the 
same  time  becoming  covered  by  the  overlying  horizontal  sandstones,  through  which 
they  appear  here  and  there  in  small  outcrops.  Farther  west  still  this  range  rises  again, 
and  where  it  joins  the  cross  ridge  at  its  western  extremity  has  become  again  bold,  with 
a  height  of  200  to  300  feet.  Although  thus  indefinite  in  its  middle  portions,  the  higher 
ground  never  entirely  disappears  along  the  line  of  the  range,  except  at  the  three  points 
where  the  Baraboo  river  and  one  of  its  tributaries  cut  through  in  deep  gorges. 

The  depressed  area  within  the  circuit  of  the  quartzite  bluffs  is,  for  the  most  part, 
somewhat  higher  than  the  surrounding  outside  country,  and  towards  its  eastern  and 
western  extremities  rises  rather  rapidly  up  to  the  enclosing  ridges.  In  Columbia  county 
much  of  the  area  between  the  ranges  is  as  high  as  the  northern  range  itself,  and  is  un- 
derlaid by  a  great  thickness  of  sandstone,  which  fills  in  the  canoe-shaped  trough  of  the 
uniting  quartzite  belts.  At  one  time  the  rest  of  the  valley  between  the  ranges  was 
filled  in  a  similar  manner,  and  has  since  been  partially  recarved  in  the  friable  sandstone 
which  still  forms  its  bottom.  This  valley  is  now  traversed  longitudinally  by  the  Baraboo 
river,  vfhich  enters  and  leaves  it  by  deep  gorges  through  the  northern  ridge,  having  a 
fall  between  the  gorges  of  about  70  feet. 

The  rock  constituting  the  great  body  of  the  Baraboo  ranges  is  a  qua,rtzite  of  a  non- 
granular,  usually  flaky,  texture,  and  of  a  color  from  nearly  white,  through  gray,  pink, 
and  amethyst,  to  purplish-red  and  even  brick-red,  the  gray  and  deep-red  being  the  most 
common,  the  white  the  least  so.  Very  rarely  a  distinct  granular  texture  is  seen,  some- 
what more  commonly  a  slight  tendency  in  that  direction.  The  quartzite  is  frequently 
very  distinctly  laminated,  the  lines  of  lamination  being  contorted  in  a  remarkable  man- 
ner, and  marked  by  alternating  light-colored  and  dark-colored  lines.  There  is  never 
any  cleavage  parallel  to  the  lamination  lines.  Next  in  abundance  to  the  regular  quartz- 
ite, and  merging  into  it,  are  heavy  beds  of  a  fine  metamorphic  conglomerate,  usually  of 
a  grayish  to  amethystine  color,  in  which  the  matrix  and  pebbles  are  alike  of  quartzite, 
and  not  always  very  well  defined  from  one  another.  Forming  thin  layers  between  the 
thick  layers  of  quartzite,  is  in  many  places  to  be  seen  a  peculiar  greasy-surfaced  quartz- 
schist,  the  laminae  of  which  are  composed  of  quartzite  like  that  of  the  regular  quartzite 
layers,  seamed  and  covered  on  the  surface  with  a  soft,  lilac  to  white,  talc- like,  mineral. 
This  slate  or  schist  usually  exhibits  the  true  slaty  or  transverse  cleavage.  The  soft 
mineral  pervading  it- is  suspected  to  be  always,  as  it  certainly  is  sometimes,  aluminous 
rather  than  magnesian.  It  occurs  occasionally  forming  slaty  layer?  with  but  little 
quartz  admixture,  and,  in  small  seams,  even  entirely  pure.  It  then  has  rather  the 
physical  characters  of  a  compacted  clay,  and  this  appearance  is  borne  out  by  the  analyses 
given  beyond,  which  show  that  the  pure  clay-like  kinds  are  probably  not  distinct  miner- 
als, but  rather  a  mixture  of  a  clayey  substance  with  fine  silica.  In  both  physical  prop- 
erties and  chemical  composition  this  material  is  closely  allied  to  the  pipestone  of  south- 
west Minnesota,  from  which  it  differs  only  in  color. 

Other  quartz-schists  of  quite  a  different  character  have  been  observed  forming  the 
lowest  layers  of  the  north  quartzite  range,  both  at  the  Lower  Narrows  of  the  Baraboo 


506  GEOLOGY  OF  CENTRAL  WISCONSIN. 

and  at  the  Upper  Narrows  of  the  same  stream.  These  are  white  to  straw-colored,  dis- 
tinctly granular  in  texture,  the  quartz  grains  being  of  translucent  glassy  quartz.  The 
whole  rock  is  more  or  less  pervaded  by  a  soft  clayey  material,  and  splits  out  in  large 
thin  sheets.  On  the  northernmost  portions  of  the  north  range,  at  the  Lower  Narrows, 
and  also  for  a  short  distance  to  the  westward,  a  great  thickness  of  quartz-porphyry  is 
to  be  observed.  This  porphyry  resembles  that  of  the  several  small  porphyry  areas  of 
the  adjoining  portions  of  Columbia,  Marquette  and  Green  Lake  counties  and  proves  at 
once  that  we  must  regard  these  areas  as  part  of  the  same  formation  that  appears  in  the 
Baraboo  ranges. 

In  the  quartzite,  milk-white  veins  and  nests  are  frequently  to  be  seen.  In  some 
places,  as  at  the  Upper  Narrows,  the  white  quartz  veins  show  frequently  geodic  cavities, 
lined  with  quartz-crystals  of  great  clearness  and  beauty,  and  not  unfrequently  of  very 
large  size,  though  usually  small.  In  the  veins  at  the  Upper  Narrows,  such  crystal - 
lined  cavities  are  exceedingly  numerous.  Along  with  the  crystals,  sometimes  compacted 
oyer  them,  sometimes  loose  in  the  cavities,  and  again  in  thin  seams  by  itself,  is  to  be 
seen  a  soft,  white  mineral.  This  is  often  pulverulent,  at  times  gritty,  at  others  a  nearly 
impalpable  powder,  and  is  shown  by  analysis  to  be  essentially  a  silicate  of  alumina. 
With  the  white  quartz,  in  nests  of  some  size,  is  often  to  be  observed  brilliant  specular 
iron  in  large  crystalline  surfaces.  It  occurs  also  in  some  of  the  layers  of  quartzite,  in 
fine  scales.  Titanic  iron  is  also  reported.  These,  with  the  peculiar  aluminous  silicate 
alluded  to  in  connection  with  the  quartz-schists,  are  the  only  minerals  known  to  occu' 
in  the  Baraboo  rocks. 

FIG.  23. 


IDEAL  SKETCH,  SHOWING  ORIGINAL  STRUCTURE  AND  AMOUNT  OF  EROSION  OP  THE  BARABOO 

RANGES. 
Scale  natural,  12,003  feet  to  the  inch.1 

The  quartzites  and  associated  rocks  are  quite  distinctly  bedded,  though  the  bedding 
is  not  unfrequently  obscured  by  cross-jointing,  which  is  often  to  be  observed  on  a  grand 
scale.  The  dip,  wherever  observed,  is  towards  the  north,  through  the  whole  extent  of 
both  ranges,  but  varies  much  in  amount.  In  the  southern  range  it  is  usually  quite 
low,  as  low  sometimes  as  15°  in  the  middle  and  broadest  portions.  In  the  northern 
range  the  dips  are  always  much  higher,  running  from  55°  to  90°.  The  rocks  of  the 
two  ranges  appear,  however,  to  be  parts  of  a  continuous  series,  the  quartz-porphyry 
beds  of  the  northern  range  constituting  the  uppermost  layers. 

For  the  relative  positions  of  the  different  ranges  and  their  relations  to  the  surround- 

1  A  sketch,  similar  to  this,  accompanies  a  paper  by  Prof.  Ohamberlin,  "  On  the  Method  of  Up- 
heaval of  the  Baraboo  Ranges,"  Trans.  Wis.  Acad.  Sci.,  Vol.  II,  but  it  is  not  drawn,  on  a  natural 
scale. 


PLATE,X.IX 


MAP 

and  C'rtva  Section*  ilhutrating  f/ir  Slrnctnrc 
cniir 

n  I«;VIL'S  LAKE  ci  o  K  o  K 

T.  II  N.  Ratitfes  VI  and  VII  E.  S  a  u  k    Co  uiit.v 

R.  D.   IrviiiCs.  l"7(v 


.  trrticn  on  line    (  ? .  D. 


Section  <>n  line    K .  F1. 


•  ^ rcl ion  en  line     O.  H.. 


Kft 


Quartzite                          Talus                     San  els 
Topography  adapted  from  maps  by  W.H.  Ciu 
Reuse  line,  of  Section*  200 feet  above  Lake  Michigan. . 
Horizontal  settle  of  Section*  anct '  Afap  I inch*  / mile  . 
Vert  icn  I  scale  /  inch  =  1500  feet . 
K.L.Le\  -el  of  DC \  //<  // uke . 

IIAVMIKKB  Imill&l •  ».-.!..  r.,,. 


mm 

Drift 


THE  ARCHAEAN  ROCKS.  507 

ing  horizontal  strata,  see  Atlas  Plate  XIV,  and  the  sections  of  Plate  XXI  of  this  vol- 
ume. If  the  view,  just  indicated,  that  there  are  no  folds  concealed  beneath  the  sand- 
stone in  the  intervening  valley,  is  the  correct  one,  the  thickness  of  the  entire  series  must 
be  very  great,  and  the  amount  of  erosion  that  has  taken  place  correspondingly  great. 
Fig.  23  indicates  the  present  structure  and  relative  positions  of  the  ridges,  and,  by  the 
dotted  lines  above,  the  possible  original  structure,  and  the  extent  of  the  erosion  that  has 
taken  place.  The  figure  is  drawn  to  a  natural  scale,  the  line  of  section  being  the  same 
as  that  of  Fig.  II  of  Plate  XX.  The  heavy  black  line  represents  the  overlying  Potsdam 
sandstone.  It  is  not  impossible  that  the  Valley  between  the  ranges  owed  its  existence, 
to  some  extent,  in  the  first  place,  to  soft  rocks  intercalated  between  the  harder  quart- 
zites.  The  hypothesis  of  Fig.  23  is  not  altogether  satisfactory.  The  entire  disappear- 
ance of  the  other  side  of  the  great  arch,  as  well  as  the  peculiar  ways  in  which  the 
ranges  come  together  at  their  extremities  are  difficult  to  explain  by  it.  It  may  be  said 
in  this  connection  that  the  dip  observations  toward  the  west  are  not  so  satisfactory  or 
numerous  as  they  might  be. 

The  irregular  areas  over  which  the  Archaean  rocks  are  at  surface,  are  indicated,  as  ac- 
curately as  present  knowledge  will  permit,  on  Atla*jPlate  XIV.  The  greatest  difficulty 
in  the  tracing  of  the  exact  boundaries  of  the  quartzite  areas  lies  in  the  fact  that  rem- 
nants of  the  horizontal  sandstones  which  flank  and  cover  them  may  be  found  at  almost 
any  elevation  upon  the  bluffs,  so  that  no  barometrical  observations  are  of  avail.  The 
areas,  as  indicated,  are,  however,  very  nearly  accurate.  There  are  places  within  them 
where,  without  doubt,  patches  of  the  covering  sandstone  occur,  but  the  quaitzite  is  in 
eveiy  such  case  but  a  short  distance  beneath.  The  peculiar  features  of  these  sandstones 
and  their  relations  to  the  other  Silurian  strata  of  the  region  are  treated  of  on  a  subse- 
quent page. 

Beginning  tlae  detailed  descriptions  at  the  best  known,  and  at  the  same  time  one  of 
the  most  remarkable,  points  about  the  quartzite  ranges,  we  note  first  the  occurrences  in 
the  vicinity  of  Devil's  Lake,  in  T.  11,  ranges  6  and  7  E.,  Sauk  county.  Here  the 
southern  range  is  cut  entirely  through  by  a  deep  quartzite- walled  valley  or  gorge,  500 
feet  in  depth,  and  three-fourths  of  a  mile  in  width.  In  its  northern  portion  this  valley 
trends  due  north  and  south  for  about  a  mile;  turning  then  abruptly  at  right  angles  it 
extends  eastward  two  miles  and  a  half.  In  the  north  and  south  part  lies  Devil's  Lake, 
with  a  length  of  something  more  than  a  mile,  and  a  width  one-fourth  less  than  this,  its 
surface  being  about  100  feet  above  the  valley  surface  at  the  eastern  end  of  the  gorge, 
more  than  100  feet  above  the  Baraboo  river  at  Baraboo,  and  more  than  200  above  tlia 
Wisconsin  at  Merrimack.  It  is  held  in  this  elevated  position  by  two  immense  morainic 
heaps  of  glacial  drift  lying  at  either  end  of  the  lake  and  rising  more  than  100  feet 
above  its  level.  The  lake  has  a  nearly  level  sandy  bottom  except  near  the  shores,  and  is 
over  most  of  its  area  some  30  feet  in  depth.  It  has  no  outlet,  and  but  one  small  stream 
running  into  it.  It  is  thus  probably  fed  chiefly  by  springs,  and  maintains  its  level  by 
evaporation  and  by  filtering  through  the  heaps  of  gravel  and  sand  which  hold  it  in 
place.  Near  the  northwest  corner  a  small  stream  running  into  the  Baraboo  passes 
within  a  few  rods  of  the  lake,  and  possibly  carries  with  it  some  of  the  lake  water. 

As  shown  on  the  map  of  Plate  XIX,  on  its  west  and  south  sides  the  lake  washes  the 
bases  of  the  bounding  cliffs  of  the  gorge.  Both  east  and  west  cliffs  are  highest  near 
their  southern  ends,  towards  which  they  rise  gradually  from  the  north,  following  roughly 
the  dip  planes,  which  also  rise  southward,  and  the  edges  of  which  can  be  seen  quite  well 
marked  on  either  wall  of  the  gorge.  By  aneroid  measurement  the  highest  point  of  the 
west  bluff  is  475  feet  above  the  lake  level  or  860  feet  above  Lake  Michigan,  and  the 
southern  portion  of  the  east  bluff  but  little  lower.  In  their  upper  portions  the  cliffs  are 
vertical,  sometimes  for  as  much  as  200  feet  or  more,  but  their  lower  parts  are  clothed 


508  GEOLOGY  OF  CENTRAL  WISCONSIN. 

with  a  heavy  talus  or  "ancle,"  composed  of  great  blocks  of  the  quartzite  that  have 
fallen  from  the  cliffs  above.  These  masses  are  often  as  much  as  20  feet  on  a  side,  with 
a  somewhat  regular  shape  imparted  by  the  powerful  joints  that  every  where  traverse  the 
quartzite,  and  cut  it  into  blocks  only  needing  to  be  slightly  dislodged  in  order  to  fall 
down  the  cliff.  For  the  greater  portion  of  their  lengths  both  east  and  west  blufft,  are 
quite  narrow,  being  backed  by  deep  ravines  opening  northward.  The  northern  end  of  the 
east  bluff,  especially,  is  a  mere  crest,  having  behind  it  one  of  the  ancient  sandstone- 
lined  ravines  that  have  before  been  mentioned. 

In  its  east  and  west  extension,  the  valley  preserves  the  same  characters  as  above  de- 
scribed, the  cliff  on  the  north  side  being  the  highest  and  boldest,  and  retaining  for  a 
long  distance  the  height  it  attains  at  the  corner  where  the  valley  bends.  Along  the  face 
of  this  cliff  the  heavy  quartzite  beds  are  seen  on  the  strike,  and  present,  therefore,  an 
appearance  of  horizon tality  when  viewed  from  the  valley  below.  At  the  mouth  of  the 
valley,  S.  E.  qr.,  Sec.  20,  T.  11,  R.  7  E,  the  northern  cliff  is  of  horizontal  sandstone, 
behind  which  the  quartzite  passes,  whilst  the  south  cliff  terminates  in  a  sharp  rocky 
point  known  as  the  Devil's  Nose .  From  the  summit  of  this  cliff,  a  short  distance  west- 
ward from  the  nose,  is  taken  the  view  on  Plate  XV.,  the  Frontispiece  of  this  report.  The 
outlook  is  northwestward  through  the  east  and  west  part  of  the  valley  to  the  lake,  be- 
yond which  the  western  cliff  of  the  lake  is  seen.  Doubling  the  nose,  we  are  on  the 
south  side  of  the  range,  with  Sauk  Prairie  in  front,  and  the  high  bluff  with  its  roclies- 
montonees  surfaces  of  quartzita  behind;  these  surfaces  rise  in  rude  steps,  which  are 
due  to  the  gradual  northern  dip. 

Near  the  top  of  the  sides  of  the  ravine  shown  by  the  map  on  the  southwest  corner  of 
the  lake,  horizontal  sandstone  and  coarse  conglomerate  occur,  the  pebbles  of  the  con- 
glomerate coming  from  the  quartzite  against  which  it  lies.  Nowhere  else  along  the 
sides  of  the  valloy  until  we  reach  its  eastern  end  are  any  indications  of  its  ever  having 
been  filled  with  sandstone,  and,  consequently,  of  its  equally  great  antiquity  with  other 
ravines  about  the  quarteite  ranges.  This  occurrence  itself  is  not  necessarily  any  such 
indication,  for  the  sandstone  is  found  only  at  a  high  level,  and  may  therefore  have  been 
introduced  from  the  northward,  quite  independently  of  the  valley  of  Devil's  Lake,  which 
we  are  thus  led  to  believe  is  of  more  recent  origin  than  the  Potsdam  period. 

This  valley  has  evidently  been  at  some  time  the  passage  of  a  large  stream.  We  can- 
not suppose  that  it  has  been  produced  by  any  other  process  than  that  of  erosion,  and 
such  an  erosion  as  could  only  b,3  effactecl  by  the  agancy  of  running  water.  Confirming 
this  view,  we  find,  high  up  on  the  cliff  sides,  within  150  feet  of  the  summit,  remnants  of 
large  potholes,  several  feet  in  diameter,  presenting  smoothed  surfaces,  and  having  about 
them  many  small  psbbles  and  smoothed  boulders  which  may  have  been  engaged  in  the 
work  of  then-  formation.  The  large  size  of  the  valley  suggests  that  it  may  have  been 
the  passage  of  the  Wisconsin  river,  which  at  the  close  of  the  Glacial  period  found  its 
ancient  channel  obstructed  by  the  great  drift  heaps  that  are  now  to  be  seen  in  it,  an:l 
was  forced  to  find  its  way  eastward  to  the  valley  of  the  great  river  that  for  long  ages 
before  the  Glacial  period  drained  the  whole  basin  of  the  Wolf  and  Upper  Fox  through 
the  valley  of  the  Lower  Wisconsin  to  the  Mississippi.  This  valley,  which  the  deflected 
river  reached  at  Portage,  and  which  it  subsequently  appropriated  as  its  own,  passes  al- 
together to  the  eastward  of  the  eastern  extremity  of  the  quartzite  ranges.  If  tin's  is  a 
correct  view,  the  river  must  have  had  a  passage  through  the  northern  range  also,  an  I 
this  passage  would  be  found  in  the  Lower  Narrows,  of  the  Baraboo,  a  much  wider 
channel  than  is  needed  by  that  small  stream.  This  explanation  of  the  origin  of  th^ 
Devil's  Lake  valley  is  offered  as  a  suggestion  only.  The  Baraboo  may  be  the  stream  t) 
which  the  work  should  be  allotted,  but,  if  so,  we  must  imagine  it  to  have  been  a  mu^'i 
larger  and  more  powerful  stream  than  now.  Only  ten  miles  above  on  its  course  t'u 
gorge  through  which  it  passes  the  northern  rang3  presents  no  such  proportions  as  se3.i 


THE  AECHJ1AN  ROCKS. 


509 


about  the  Devil's  Lake  valley.    For  a  further  idea  of  the  structure  of  this  valley  refer- 
ence is  made  to  the  sections  of  Plates  XIX  and  XX. 

The  rock  in  the  vicinity  of  Devil's  Lake,  omitting  reference  now  to  the  Silurian  con- 
glomerate and  sandstones,  is  nearly  altogether  the  typical  quartzite  of  the  region,  as 
above  described.  It  generally  shows  some  shade  of  red.  On  the  weathered  surfaces  of 
some  of  the  large  f  alien  masses  in  the  edge  of  the  lake,  a  distinct  tendency  to  a  granular 
texture  is  perceptible,  whilst  a  fresh  surface  shows  generally  no  traces  of  it.  Fine  lines 
of  lamination  are  nearly  everywhere  to  be  seen,  and  are  generally  quite  strikingly 
marked,  but  there  is  never  any  structure  parallel  to  them.  They  are  nearly  always  bent 
into  sharp  angles,  or  curved  and  contorted,  presenting  often  the  irregularities  seen  in 
the  bedding  of  sandstone.  Whilst  many  of  the  bendings  in  these  lines  may  be  due  to 
original  irregularities  of  deposition,  or  to  contortion  at  the  time  of  disturbance  and  alter- 
ation, there  are  surfaces  where  they  present  such  a  peculiar  knotty  and  concentric  ap- 
pearance as  strongly  to  suggest  a  concretionary  origin.  A  portion  about  3  feet  square 
of  such  a  surface  is  figured  in  Fig.  24.  The  lines  are  alternatingly  light  and  dark  red. 

FIG.  24. 


SURFACE  or  QUARTZITE  SHOWING  CURVED  LAMINATIOW. 

In  a  few  places  white  quartz  veins  with  geodic  quartz  crystals  are  seen,  but  these  do  not 
characterize  any  considerable  portion  of  the  rock.  All  about  the  Devil's  Lake  valley  the 
bedding  of  the  quartzite  is  quite  distinct,  and  is  made  apparent  by  the  existence  of  large 
dip  surfaces,  often  beautifully  ripple-marked.  At  the  northern  ends  of  both  east  and 
west  bluffs  of  the  lake  many  such  surfaces  occur.  Others  are  seen  on  the  sides  of  the 
railroad  track  about  midway  the  length  of  the  lake.  These  all  give  an  inclination  to  the 
north  of  15°  to  25°,  the  higher  figure  being  seldom  reached,  and  a  strike  of  N.  80°  E. 
The  quartzite  layers  are  many  feet  in  thickness,  showing  no  internal  structure  whatever 
parallel  to  the  general  dip  direction,  but  being  affected  everywhere  by  the  curved  and 
bent  lamination  alluded  to.  Between  the  quartzite  beds  occur  layers  of  greasy  quartz- 
slate,  usually  but  a  few  inches  in  width.  Such  a  layer  is  well  exposed  on  the  side  of  the 
railroad  track  on  the  east  side  of  the  lake,  the  laminae  dipping  N.  37°,  or  transverse  to 
the  bedding  planes.  The  slate  is  quartzite,  like  that  of  the  surrounding  beds,  but  is 
penetrated  by  a  soft,  greasy  mineral,  and  affected  by  slaty  cleavage.  As  the  cleavage 
planes  of  the  slate  approach  the  surface  of  the  adjoining  quartzite,  they  curve  towards 
and  penetrate  it  to  a  short  distance,  as  indicated  in  Fig.  25.  Large  surfaces  of  quartzite, 


510 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


which  have  had  one  of  these  slaty  layers  removed  from  above  them,  show  a  peculiar 

ridgy  appearance,  evidently  due  to  the  passage  into  them  of  the  slaty  cleavage  planes. 

At  the  summit  of  the  east  bluff,  near  its  southern  end,  indications  of  a  somewhat 

lower  dip  than  elsewhere  are  seen,  whilst  at  the  Devil's  Nose,  surfaces  occur  slanting  as 


FIG.  25. 


much  as  29°  northward.  At  the  latter  place,  many 
cross-joints  obscure  the  bedding,  nearly  all  of  the 
planes,  however,  sloping  northward.  Some  very 
large  ones  were  noted,  with  as  high  an  angle  as  82°, 
covered  with  a  shining,  soft,  greasy  film.  In  seams 
and  nests  in  the  quartzite,  in  this  vicinity,  occurs 
a  compact,  but  soft,  clay-like  substance  (1254)  of  a 
lilac  color,  which  is  penetrated  by  fine  white  strings, 
and  con  tains:  silica,  62.16;  alumina,  29.67;  iron  ox- 
ide, 4.17;  lime,  0.16;  water,  2.50=99.36.  This  sub- 
stance appear  to  be  the  same  as  that  which  per- 
vades and  gives  character  to  the  quartz-schists  of 
the  region,  and  is  closely  allied  to  the  red  "  pipe- 
stone,"  that  occurs  with  the  quartzites  of  Barron 
county,  and  again  in  southwest  Minnesota. 
On  the  summits  and  sides  of  all  the  cliffs  about  the  lake  and  valley,  two  sets  of  very 
marked  vertical  cross-joints  are  to  be  seen,  the  more  prominent  and  persistent  set  trend- 
ing N.  45*  W.  These  joints  have  produced,  on  the  upper  portions  of  the  cliffs,  a  striking 
columnar  appearance,  the  separate  columns  of  quartzite,  20  to  40  feet  in  height,  often 
standing  entirely  detached  by  the  joint  cracks  from  the  main  cliff.  In  some  cases,  in- 
tervening masses  of  quartzite  have  fallen,  and  left  entirely  isolated  needles  at  a  distance 
from  the  cliff  face. 

As  in  the  ravine  at  the  southwest  corner  of  the  lake,  so  also  in  many  other  places  on 
the  north  flank  of  the  ridge,  horizontal  ledges  of  sandstone  and  very  coarse  conglomer- 
ate occur,  abutting  against,  and  unconformably  overlying  the  quartzite.  At  the  north- 
ern point  of  the  east  bluff,  the  contact  of  the  two  formations,  is  beautifully  exposed,  and 
the  very  instructive  section  represented  in  Fig.  26  occurs.  Here  the  ends  of  columnar, 

FIG.  26. 


SLATY  CLEAVAGE  IN  QUABTZ  SLATE  AT 
DEVIL. 'SLAKE. 


POTSDAM  BOWLDER-CONGLOMERATE  AND  SANDSTONE  ON  AROH.BAN  Q.UAKTZITE,  DEV-IL'S  LAKE 

Scale,  ten  feet  to  the  inch. 
A.  B  ,  Quartzite.    B.  C.,  Sandstone.    C.  D.,  Qnartzite.    D.  E.,  Sandstone. 


THE  ARCILEAN  ROCKS.  511 

joint- detached,  masses  of  the  quartzite  are  surrounded  and  filled  between  by  the  hori- 
zontal sandstone,  the  whole  capped  with  a  heavy  layer  of  a  conglomerate  composed  of 
angular,  subangular,  and  rounded  masses  of  quartzite,  embedded  in  a  coarse,  friable, 
sandy  matrix,  which  is  occasionally  cemented  by  the  brown  oxide  of  iron,  and  is  not 
unfrequently  almost  altogether  excluded  by  the  included  boulders.  The  quartzite  of  the 
boulders  and  pebbles  is  the  same  as  that  of  the  ledges  further  up  the  bluff.  Places  also 
occur,  as  shown  in  the  figure,  where  the  sand  and  quartzite  pebbles  are  wedged  down 
into  the  joint-cracks  of  the  quartzite. 

Eastward  from  the  mouth  of  the  Devil's  Lake  valley,  in  Sec.  29,  T.  11,  R.  7  E,  the 
southern  face  of  the  quartzite  range  continues  high  and  bold  on  the  right  hand,  as  far 
as  Sec.  25,  T.  12,  R.  8  E.,  in  Columbia  county.  On  Mr,  Fitsimmons'  place,  on  Sec.  22, 
T.  11,  R.  7  E.,  Sauk  county,  near  Parphrey's  glen,  and  only  a  short  distance  from  the 
south  slope  of  the  ridge,  one  of  the  highest  points  on  the  whole  range  of  bluffs  occurs, 
the  elevation  being  nearly  100  feet  greater  than  that  of  the  Devil's  Lake  bluffs.  The 
point  is  in  use  by  the  United  States  Coast  Survey,  as  a  signal  station.  North  from  the 
signal  station,  the  quartzite  range  has  a  width  on  top  of  nearly  three  miles.  As  far  as 
Sec.  3,  T.  11,  R.  8  E.,  Columbia  county,  the  south  face  of  the  range,  except  at  the 
higher  levels,  where  large  surfaces  of  bare  quartzite  occur,  is  composed  of  sandstone, 
with  some  coarse  conglomerate,  which  flanks  the  quartzite  in  horizontal  layers.  These 
flanking  sandstones  are  well  exposed  at  the  mouth  of  the  Devil's  Lake  gorge;  in  Par- 
phrey's glen,  on  the  line  between  sections  23  and  22,  T.  11,  R.  7  E.,  Sauk  county;  and 
again  in  Dorward's  or  St.  Mary's  glen,  on  the  line  of  sections  18  and  7,  T.  11,  R.  8  E., 
Columbia  county.  In  all  these  places,  the  sandstone  layers  appear  to  possess  a  small 
dip,  about  5°,  away  from  the  quartzite  core.  At  Dorward's  Glen,  the  quartzite  is  to  be 
seen  at  the  north  end  of  the  gorge,  and  lying  upon  and  against  it  sixty  feet  of  horiz- 
ontal sandstone  and  bowlder-conglomerate,  as  shown  in  Fig.  27.  These  are  ex- 
posed on  the  wall  of  the  gorge,  the  conglomerate  forming  the  base  of  the  cliff  and 
the  stream  bed,  with  a  thickness  seen  of  four  feet.  The  bowlders  of  the  conglomerate 
are  largely  irregular,  angular  masses  reaching  up  to  eight  inches  in  size,  and  are 
almost  entirely  without  surrounding  matrix.  The  quartzite  at  the  head  of  the  glen  is 
non-granular,  pinkish-gray  to  red,  and  without  plain  bedding. 

FIG.  27. 


SANDSTONE  AND  CONGLOMERATE  ON  QUARTZITE  AT  DOKWARD'S  GLEN. 
Scale  90  feet  to  the  inch. 

East  of  Sec.  3,  T.  11,  R.  8  E.,  as  far  as  the  end  of  the  range,  the  flanking  sandstone 
appears  to  be  wanting,  outcrops  of  quartzite  in  places  extending  from  summit  to  base  of 
the  southern  face  of  the  range.  Such  a  place  occurs  on  the  northern  side  of  Sec.  3,  and 
southern  side  of  Sec.  34,  T.  12,  R.  8  E.,  near  Mr.  Fleming's  house.  Here  the  quartzite 
bluff  rises  immediately  from  the  north  side  of  the  Portage  road,  showing  for  the  first 
steep  ascent  of  250  feet,  large  loose  masses  and  rough  exposures  of  a  metamorphio 
conglomerate,  in  which  matrix  and  pebbles  are  both  of  quartzite,  the  pebbles  being  very 
small  and  in  no  way  different  from  the  matrix.  From  the  top  of  this  slope  a  gradually 
rising  wooded  step  is  crossed  for  about  a  tliird  of  a  mile  to  a  second  nearly  precipitous 


512  GEOLOGY  OF  CENTRAL  WISCONSIN. 

rise  of  over  a  hundred  feet.  The  summit  is  of  bare  rock,  and  is  a  mere  crest,  others 
similar  to  it  occurring'  east  and  west  along  the  range.  The  bedding  of  the  quartzite  is 
distinct,  the  strike  being  N.  63°  E.,  and  dip  60°  N. 

On  Sees.  34,  35,  26  and  27,  T.  12,  R.  8  E.,  numerous  other  large  quartzite  exposures 
occur.  On  the  S.  E.  qr.  of  Sec.  27,  large  outcrops  on  the  roadside  show  pinkish -gray, 
opaque  quartzite  (755)  with  very  fine  greenish-black  streaks  (Mica?). 

The  eastern  end  of  the  quartzite  ranges  is  on  Sec.  25,  T.  12,  R.  8  E.,  where  the 
two  ranges  -unite  in  the  bold  point  that  has  been  heretofore  alluded  to.  On  the  north 
side  of  the  point  the  horizontal  sandstone  begins  again  to  flank  the  quartzite.  On  the 
N.  W.  qr.  of  Sec.  25,  the  road  ascending  the  bluff  shows  sandstone,  with  a  slight  slant 
eastward,  nearly  to  the  top.  Near  by,  on  the  S.  E.  qr.  of  N.  E.  qr.  of  Sec.  26,  are  large 
rounded  exposures  (roches  montonees)  of  quartzite  showing  on  the  top  glacial  furrows 
and  scratches,  and  also  several  large  smoothed  potholes,  the  largest  two  feet  wide  and 
one  foot  deep,  with  connecting  furrows.  Occurring  where  no  stream  could  now  possibly 
run,  these  potholes  are  of  interest  as  showing  the  great  erosion  the  quartzite  must  ha,ve 
undergone  since  their  formation. 

Along  the  northern  side  of  the  north  range  and  westward  from  the  eastern  ex- 
tremity, the  flanking  sandstone  continues  nearly  to  the  county  line.  On  the  south  side 
of  section  23,  well  up  on  the  bluff,  a  steep  ravine  has  laid  bare  the  sandstone  and  quartz- 
ite nearly  in  contact,  as  shown  in  Fig.  28.  The  quartzite  here  (753)  is  a  fine  metamor- 

FIG.  28. 


UNCONFORMABILITY,  SEC.  23.    CALEDONIA. 

phic  conglomerate,  in  which  the  matrix  of  pinkish-white  quartz  embraces  darker-hued 
pebbles  TV  inch  to  \  inch  in  diameter.  The  pebbles  are  very  firmly  attached  to  the 
matrix,  and  are  not  always  well  defined  from  it.  Nests  and  veins  of  white  quartz  (754) 
occur  in  this  rock. 

On  the  N.  E.  qr.  of  sec.  22,  T.  12,  R.  8  E.,  a  deep  ravine  shows  a  great  thickness  of 
sandstone,  with  a  bed  of  bowlder  conglomerate,  dipping  northward,  or  away  from  the 
qnartzite.  Further  westward  along  the  road  from  Portage  to  Baraboo,  which  follows 
the  foot  of  the  bluff,  sandstone  is  seen  in  numerous  places.  On  the  N.  W.  qr.  of  Sec.  21, 
high  up  on  the  bluff,  a  well  goes  through  10  feet  of  sandstone  and  then  into  quartzite. 
It  is  quite  probable  that  the  quartzite  core  is  in  places  along  here  entirely  covered  by 
Siindstone.  The  core  does  not  extend,  however,  beyond  the  southern  line  of  sections  19, 
20,  and  21,  for  here  wells  pass  through  over  170  feet  of  sandstone.  After  passing  the 
county  line,  the  north  slope  of  the  quartzite  is  again  free  from  its  sandstone  mask,  and 
is  to  be  seen  in  small  outcrops  dipping  N.  60°. 


THE  ARCILEAN  ROCKS. 


513 


MAP  OP  THE  LOWER  NARROWS  OF  THE  BARABOO. 
Scale  iy2  inches  to  the  mile. 


On  Sections  23  and  26,  T.  12,  R.  7  E.,  Sauk  county,  theBaraboo  river  passes  the  north 
qaartzite  range  in  a  gorge  known  as  the  Lower  Narrows  of  the  Baraboo.     Fijr  29 

indicates  the  topography  and  points  of 

FIG.  29.  interest  in  the  vicinity  of  the  Narrows. 

The  passage  is  nearly  half  a  mile  in 
width,  the  level  bottom  extending  to  the 
fooc  of  the  cliffs  on  either  side.  The 
cliffs  rise  400  feet  above  the  river,  and 
show  finely  the  great  beds  of  quartzite, 
and  associated  strata.  The  gorge  is 
much  wider  than  needed  by  the  small 
stream  that  now  occupies  it,  and  may, 
as  already  suggested,  have  been  at  one 
time  used  by  the  Wisconsin,  as  the  val- 
ley of  Devil's  Lake  seems  to  have  been. 
It  is  unlike  the  latter  valley  in  having 
been,  in  part  at  least,  formed  first  before 
the  Potsdam  period,  as  indicated  by  the 
way  in  which  horizontal  sandstone  and 
conglomerate  ledges  occur  around  the 
heads  of  steep  ravines  that  extend  down 
the  cliff  towards  the  main  gorge.  Fig. 
30  is  a  section  north  and  south  through 
the  west  bluff'  at  the  Narrows.  It  is  a  combination  of  a  paced  section  made  along  the 
west  line  of  sections  23  and  26,  and  of  another,  not  so  carefully  measured,  made  about 
40  rods  further  west.  The  first  follows  closely  the  edge  of  the  cliff,  where  the  quartzite 
beds  are  exposed  to  the  southern  edge  of  the  ridge,  the  other  runs  a  little  west  of  north 
from  Mrs.  Garrison's  house,  in  the  N.  E.  qr.  of  Sec.  27,  and  passes  for  a  long  distance  over 
horizontal  sandstone  and  conglomerate  layers  filling  an  old  ravine  in  the  quartzite.  The 
scale  of  the  figured  section  is  a  natural  one,  and  the  contour  indicated  is  quite  closely 
that  of  the  range  on  the  westernmost  of  the  two  lines. 

Beginning  with  the  north  end  of  the  section,  we  find,  forming  the  north  face  of  the 
range,  in  bold  northward  sloping  ledges,  quartz-porphyry  about  600  feet  in  width. 
This  porphyry  (1244,  1252)  is  for  the  most  part  dull-red  to  pinkish  on  the  weathered 
surface,  which  is  a  good  deal  altered,  often  iron-stained,  and  has  generally  a  whitish 
undercrust.  The  least  altered  specimens  show  a  brownish-pink  matrix,  through  which 
are  scattered,  very  thickly,  large  facets,  up  to  %  inch  in  diameter,  of  bright-red  cleava- 
ble  felspar,  and,  more  sparsely,  minute  facets  of  a  white  kind.  In  nearly  all  speci- 
mens a  few  small  greenish-black  blotches,  apparently  composed  of  fine  mica  scales, 
occur,  as  also  small  iron-stained  cavities,  which  often  show  linings  of  minute  quartz- 
crystals.  The  porphyry  is  very  distinctly  bedded,  showing  an  E.  W.  strike,  and  a  dip 
of  58°  to  60°  N.  Towards  its  lowest  portions,  and  higher  up  on  the  bluff,  it  becomes 
gradually  more  slaty  in  character  (1245  and  1245a),  the  felspar  facets,  though  very  nu- 
merous, becoming  at  the  same  time  less  well  defined,  and  the  surfaces  of  the  laminae 
becoming  covered  with  a  soft  greasy  mineral.  This  finally  changes  to  a  distinct  schist, i 
about  80  feet  wide,  containing  a  large  proportion  of  the  soft  mineral,  and  allied  to  the 
greasy  quartz-schists  occurring  at  Devil's  Lake,  but  without  transverse  cleavage.  Con- 
tinuing the  ascent  of  the  bluff  southward,  quartzite  is  seen  lying  immediately  under- 
neath the  schist,  and  forming  the  body  of  the  ridge  to  the  foot  of  its  southern  slope. 
At  first  this  quartzite  is  much  veined  and  seamed  with  reticulating  veins  of  white 
quartz,  in  which  fine  specular  iron  is  occasionally  to  be  seen.  At  the  summit  of  the 

i  Thi'  <"-hist  is  probably  non-magnesian,  like  the  schists  of  Devil's  Lake,  ordiuarily  called  talcose. 
Wis    Sen.  —  33 


614 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


a  2 


ta  02 


hill  this  character  is  less  marked,  and  the  rock  (1253)  is  a  dark 
reddish-purple  quartzite  with  a  distinct  tendency  to  a  granular 
texture,  the  individual  grains  being  vitreous  and  translucent, 
but  the  rock  as  a  whole  having  a  dull,  opaque  appearance.  The 
bedding  of  the  quartzite  is  not  everywhere  very  plain.  Towa  rds 
the  north  the  layers  appear  to  conform  to  the  directions  noticed 
in  the  overlying  porphyry,  but  further  southward  the  inclination 
is  much  steeper,  and  on  the  south  slope,  near  the  end  of  the 
ridge,  beautifiully  ripple-marked  vertical  surfaces  are  seen.  In- 
terstratified  with  the  quartzite  in  places  are  some  greasy- sur- 
faced schistose  layers.  At  the  foot  of  the  hill,  near  Mrs.  Gar- 
rison's house,  the  low  est  member  of  the  series  is  seen  in  a  pecu- 
liar white  to  straw-colored  quartz-schist  or  slate  (1284).  This 
slate  occurs  in  regular  smooth-faced,  brown-tinted,  layers,  ^th 
inch  to  3  or  4  inches  in  thickness,  and  has  a  fine  granular  tex- 
ture, the  grains  being  of  more  or  less  angular  quartz.  Sur- 
rounding the  grains  and  pervading  the  mass  is  a  fine  white 
pulverulent  matrix,  which  renders  the  rock  soft,  and  has  ti 
highly  argillaceous  odor  when  breathed  upon.  Only  about  15  to 
20  feet  are  exposed.  The  northward  dip  is  very  plain,  the 
edges  of  the  layers  in  places  'being  much  bent  out  of  the  true 
inclination,  which,  as  seen  in  the  old  shaft  near  by,  is  as  much 
as  60°  to  70°.  The  whole  thickness  of  the  metamoqjhic  rucks 
represented  in  this  section  is  not  far  short  of  5,000  feet. 

A  short  distance  westward,  and  a  few  feet  above  the  quartz- 
schist  just  described,  horizontal  sandstone  is  quarried.  Further 
up  the  bluff,  this  is  succeeded  by  a  great  thickness,  probably 
a  hundred  feet,  of  a  horizontally  bedded,  coarse  bowlder-con- 
glomerate, the  bowlders  chiefly  of  red  quartzite  from  the  rocks 
near  by,  and  the  matrix  usually  a  loose  friable  sand.  The  con- 
glomerate rises  nearly,  or  quite,  to  the  summit  of  the  ridge. 

The  east  bluff  of  the  Narrows  does  not  present  so  fine  a  sec- 
tion as  the  one  just  described;  the  exposures  are,  however,  very 
large.  At  the  south  point  of  the  cliff,  the  elevation  is  310  feet 
above  the  Baraboo,  and  the  rock  a  veiy  compact,  red-tinged, 
slightly  vitreous  quartzite.  Near  the  middle  of  the  cliff,  a  very 
steep  ravine  indents  its  face.  On  the  south  side,  and  around  the 
head  of  the  ravine,  are  horizontal  ledges  of  a  conglomerate  of 
quartzite  pebbles  up  to  6  inches  in  diameter,  for  the  most  part 
without  matrix.  What  matrix  is  present  appears  in  many 
places  to  be  almost  as  much  of  a  quartzite  as  the  pebbles  them- 
selves, though  in  others  it  is  sandy  and  friable.  On  the  north 
side  of  the  ravine,  semi-translucent,  amethystine  quartzite  is 
seen,  unconcealed  by  conglomerate.  Further  northward,  the 
steep  N.  70°  dip  of  the  quartzite  is  very  plain,  the  dip  surfaces 
being  often  laid  bare  for  a  great  distance,  and  giving  a  very 
steep  slope  to  the  north  side  of  the  ridge.  The  east  cliff  of  the 
Narrows  does  not  extend  so  far  north  as  that  on  the  wesf . 

West  from  the  Narrows,  for  about  two  miles,  the  north 
face  of  the  range  .trends  north  of  west,  continuing  to  show  all 
along  beds  of  quartz-porphyry.  Since  the  strike  throughout  is  E. 
W.,  the  existence  of  a  very  much  broader  belt  of  porphyry  than 


THE  ARCH^AN  ROCKS. 


515 


FIG.  31. 


shown  in  the  Narrows  section  is  indicated.  On  the  south  side  of  the  S.  E.  qr.  of  Sec.  16, 
the  porphyry  reaches  its  northernmost  point,  showing  in  a  bold  rocky  projection.  The 
rock  here  (1,242)  presents  a  dull-brownish  appearance  on  a  weathered  surface,  and  is 
much  fissured  by  weathering,  the  surfaces  of  the  fissures  showing  generally  a  brownish 
iron  stain.  A  schistose  structure  is  apparent  in  places,  and  the  bedding  is  plain,  with  an 
E.  W.  strike,  and  dip  of  55°  N.  A  fresh  fracture  shows  a  compact,  flaky  matrix,  of 
dark- brown  to  nearly  black,  sometimes  grayish  color,  the  last  being  characteristic  of  al- 
tered portions.  The  color  is  not  quite  uniform,  but  is  mottled  with  fine  strings  and 
specks  of  whitish  or  pinkish  color,  and  of  indefinite  outline.  This  matrix  fuses  easily  to 
a  black  glass.  In  altered  specimens  it  is  easily  scratched  by  the  knife,  in  unaltered  ones 
the  knife  makes  almost  no  impression.  Sparsely  scattered  through  it  are  minute  white 
and  pink  felspar  facets,  and  still  fewer  large  brick-red  ones.  In  this  regard  the  rock  is 
quite  different  from  that  of  the  Narrows  section. 

About  one-eighth  to  one-fourth  of  a  mile  eastward  from  this  rocky  point,  in  the  N.  E. 
qr.  of  the  N.  E.  qr.  of  Sec.  21,  the  porphyry  is  seen  again  in  a  large  exposure,  showing 
the  same  weathered  appearance,  and  bedding  structure.  Specimens  from  this  place 
(1,248)  resemble  the  rock  last  described,  having  somewhat  more  numerous  felspar  facets, 
and  containing:  silica,  71.24;  alumina,  12.20;  iron  peroxide,  1.71;  iron  protoxide,  5.44; 
lime,  0.98;  magnesia,,  0.13;  magnanese  oxide,  0.97;  potash,  1.86;  soda,  4.29;  water,  0.81 
=99.63.  The  large  content  of  soda,  as  compared  with  potash,  is  noteworthy. 
The  quartz-porphyries  have  thus  been  traced  along  the  north  flank  of  the  range  from 
the  Baraboo  Narrows,  in  Sec.  23,  to  the  south  side  of  Sec.  16. 
Judging  from  the  bedding  directions,  their  whole  width  can- 
not be  less  than  three-fourths  of  a  mile,  nor  their  actual  thick- 
ness short  of  3,200  feet.  They  are  found  nowhere  else  in 
the  Baraboo  region.  From  the  descriptions  and  analysis  given 
it  will  be  seen  that  these  rocks  have  a  matrix  too  sih'cious  to 
be  purely  felspathic,  through  which  are  scattered  crystals  of 
orthoclase,  possibly  also  of  a  soda  felspar,  the  porphyritic 
quartz  crystals  generally  characteristic  of  quartz-porphyry  be- 
ing absent.  They  are  evidently  nearer  to  true  quartz-porphy- 
ry, however,  than  to  the  non-sihcious  porphyrites.1 

Further  west  again,  and  until  we  reach  the  Upper  Nar- 
rows of  the  Baraboo,  in  the  town  of  Excelsior,  the  quartzite 
exposures  along  the  north  range  are  only  occasional,  as  on  the 
low  ridge  north  of  Baraboo,  and  on  the  N.  E.  qr.  of  Sec.  33, 
T.  12,  R,  6  E. 

On  Sees.  28  and  29,  T.  12,  R.  5  E.,  in  the  town  of  Excel- 
sior, the  Baraboo  river  breaks  southward  through  the  north 
quartzite  range  in  a  narrow  gorge,  200  feet  in  depth,  and 
something  more  than  half  a  mile  in  length,  known  as  the 
Upper  Narrows  of  the  Baraboo.  For  most  of  its  length 
e  the  ravine  is  just  wide  enough  to  admit  of  the  passage  of  the 
river,  railroad  and  a  wagon  road.  Here  the  quartzite  core  of 
the  north  range  is  finely  shown,  flanked  on  either  side,  and  even  overtopped,  by  the 
horizontal  sandstone  and  conglomerate.  Fig.  31  is  a  map 5  showing  the  shape  and 
character  of  the  gorge.  Fig.  32  is  a  section  on  the  line  A  B  C  of  Fig.  31,  drawn  to  a 
horizontal  scale  of  750,  and  a  vertical  of  300  feet  to  the  inch.3 

i  Von  Cottas  I.ithclogy,  pp.  168  and  214. 
4  Copied  from  M;-.  W.  H.  Oanfleld's  map  of  Excelsior. 

'  In  Fig.  32,  the  inclined  lines  in  the  "  veined  quartzite  "  are  meant  for  shading  only,  and  do  not 
indicate  any  structure  to  the  rock,  which,  as  described,  is  without  distinct  bedding, 


UPPER  NARROWS  OF  THE 
BARABOO. 

Scale,  iy2    inches 
mile. 


516 


GEOLOGY  OF  CENTRAL  WISCONSIN, 


SI 


«  "bi 


quartzite  is  indistinct. 
North  of  and  overly 


At  the  southern  end  of  the  section  —  the  "Jaws  of  the 
Narrows  "  —  horizontal  sandstone  layers,  altematingly  hard 
and  quartzitic,  and  soft  and  friable,  are  seen  abutting 
against  and  overlying  heavy  beds  of  north  ward- sloping, 
pinkish-gray,  dark-gray,  and  purple,  vitreous  quartzite 
(1273,  1274).  The  exact  contact  of  the  two  formations  is 
finely  exposed,  the  sandstone  filling  the  cracks  between  the 
layers  of  quartzite  and  including  large  detached  masses  of 
the  latter  rock.  A  short  distance  northward,  along  the  wall 
of  the  gorge,  this  quartzite  is  terminated  by  a  steep  ravine, 
on  the  north  side  of  which  comes  in  the  veined  quartzite 
that  forms  the  body  of  the  ridge.  This  curiously  veined 
rock  (1267,  1275)  may  be  described  as  a  light  to  dark-red- 
dish, sometimes  purple,  usually  somewhat  vitreous,  quartz- 
ite, which  has 
been  shattered  FIG.  33. 

g  &  throughout  into 
-e    small,  sharply 

-q    angular  frag- 

J  3    ments,    and 

|j  *~  these  cemented 

00  jT  together  again 

£  S   by  milky-white 

.515   vein  quartz,  the 

j|  *   numerous  cavi- 

«5    ties    in    which 

8.2 

8 1   are  lined   with 

a,  o-  small,  brilliant, 

03     .. 

,«"  and  very  per- 
_;  ••«  feet  quartz  crys- 
^S  tals.  The  ex- 
£.«  tensive  fissuring 
3 '3  to  which  this 
g  |  rook  has  been 

c.j^  subjected  is  indicated  not  only  in  the  interlacing  veins  of 

1'|   white  quartz,  which  often  make  up  half  the  mass,  but  al- 

E  £  so  in  the  frequent  juxtaposition  of  different  looking  f  rag- 

7,s5   ments  of  the  quartzite.     Certain  portions  of  the  rock  are 

jsj    more  fissured  than  other  neighboring  portions,  and  then 

.§  91  appear  like  wide  veins  into  which    numerous    fragments 

o  "   of  the  wall  rock  have  fallen.    Fig.  33  represents  a  small 

"g  g  area,  two    feet  by  one  and  a  half    feet,    of    the  veined 

a3-  quartzite,    the    white    representing    the    vein-quartz,    the 

£*   black  the  fragments  of  red  quartzite.     In  some  of  the  crys- 

«      tal-lined  cavities  a  soft  white  coating  is  noticed  on  the  crys- 

Q,      tals.    The  same  material  is  seen  sometimes  lying  loose  in 

^      the  cavities  and  again  filling  minute  cracks  in  a  more  com- 

r      pacted  condition.     According  to  Prof.  Daniells'  analysis  it 

contains  silica,  53.15  per  cent ,  and  alumina,  45.09  per  cent., 

the  balance  being  water.    The  bedding    of*    the    veined 

It  appears  to  stand  at  a  high  angle  to  the  northward. 

ing  the  veined  rock  is  another  bait  of  quartzite  (1277)  without 


-farilie 


VEINED  QUABTZITE. 


THE  ARCILEAN  ROCKS.  517 

veins,  of  a  pinkish  color,  and  containing  much  of  the  greasy,  talc-like  mineral,  which, 
in  places,  imparts  a  highly  schistose  character  to  the  rock,  sometimes  predominating 
over  the  quartz.  In  these  cases  the  slaty  laminae  incline  westward  15°,  whilst  the  whole 
rock  is  intersected  by  E.  W.  planes  standing  at  nearly  90°.  The  schistose  layers  are 
only  in  the  upper  portion  of  the  belt  which  further  south  is  purer  quartzite  with  an  evi- 
dent northward  dip. 

As  indicated  in  the  figure,  the  quartzite  is  over-topped,  for  nearly  the  whole  length 
of  the  section,  by  horizontal  sandstone  and  conglomerate  layers.  The  conglomerate 
capping  the  bluff  in  its  lu'gher  portions,  and  overlying  the  veined  quartzite,  shows  a 
mass  of  pebbles  and  small  bowlders  of  the  veined  rock,  compacted  together  without 
matrix,  or  with  one  that  is  very  hard  and  quartzite-like,  and  of  a  brownish  color.  A 
fine  exposure  of  this  conglomerate  is  to  be  seen  at  the  top  of  the  cliff,  at  a  point  just 
east  of  the  southernmost  of  the  two  railroad  bridges  within  the  Narrows,  and  on  the 
south  side  of  the  bend  which  both  gorge  and  river  here  make  to  the  eastward.  At  the 
top  of  the  cliff,  on  the  north  side  of  the  bow,  140  feet  above  the  railroad  track,  sand- 
stone, partly  hard  and  brownish,  with  a  vitrified  appearance,  and  partly  friable,  is  un- 
derlaid by  horizontal  ledges  of  a  conglomerate,  having  a  hard  quartzite  matrix,  and 
including  red  quartzite  pebbles  and  bowlders  of  all  sizes.  Twenty-five  feet  below  the 
top  of  the  cliff,  the  junction  of  the  conglomerate  with  the  underlying  vertically-bedded 
quartzite  is  seen.  As  viewed  from  the  track  below,  the  unconformability  is  very  striking. 
The  conglomerate  extends  northward  from  this  point,  and  down  the  side  of  the  ravine 
next  north  of  the  bend  of  the  river,  to  within  30  feet  of  the  railroad  track.  Its  lower 
portions  (1278)  show  a  loose,  friable,  biownish  matrix  of  coarse  sand,  the  quartzite  peb- 
bles running  up  to  a  foot  in  diameter,  but  being  usually  smaller  than  this.  Below  the 
conglomerate,  and  abutting  directly  upon  the  railroad  track,  is  a  cliff  '20  to  30  feet  high, 
of  coarse,  brownish,  friable  sandstone,  without  pebbles,  showing  cross-lamination  on  a 
grand  scale.  North  of  the  ravine,  a  low  sandstone  ridge  is  capped  by  the  lower  layers 
of  bowlder-conglomerate. 

On  Sec.  31  of  the  town  of  Excelsior,  is  another  gorge,  known  as  the  Narrows  of 
Narrows  Creek.  In  its  structure  and  rock  occurrences,  this  gorge  is  similar  to  the 
Narrows  of  the  Baraboo,  the  veined  quartzite,  however,  being  less  developed  than  at 
the  latter  place.  Between  the  two  gorges  the  summit  of  the  range  is  quite  level. 

Westward  from  the  passage  of  Narrow's  Creek,  the  north  quartzite  range  curves  south- 
ward to  meet  the  north  and  south  ridge  that  connects  it  with  the  southern  or  main 
range.  In  the  road  near  the  center  of  Sec.  36,  T.  12,  R.  4  E.,  Reedsburg,  well  up  on 
the  ridge,  quartzite  is  exposed  with  an  E.  W.  strike  and  dip  of  N.  70°.  This  is  its  north- 
ern limit,  and  the  western  end  of  the  range,  for  just  west  of  the  road  a  rocky  ravine, 
over  100  feet  in  depth,  shows  the  quartzite  flanked  on  the  north  by  heavy  beds  of  coarse 
conglomerate  and  friable  sandstone,  the  quartzite  occurring  only  on  the  eastern  wall  of 
the  ravine,  the  western  side  being  altogether  of  sandstone. 

South  from  the  center  of  Sec.  36,  along  the  connecting  ridge,  the  ground  rises  steadily 
for  several  miles.  For  the  first  mile,  horizontal  sandstone  ledges  are  seen  rising  to  an 
elevation  of  520  feet.  In  the  north  part  of  Sec.  13,  T.  11,  R.  4  E.,  Westfleld,  eleva- 
tions of  over  600  feet  are  reached.  In  this  vicinity,  and  over  a  considerable  area  in  sec- 
tions 11,  12,  13,  14,  23  and  24,  low  outcrops  of  quartzite  occur,  the  area  including  them 
being  all  very  high,  and  constituting  a  rounded  swell  above  the  general  level.  A  long, 
lovr  outcrop  near  the  Lutheran  church  in  S.  W.  qr.  Sec.  13,  shows  dark,  purplish-red, 
flaky-textured  quartzite  (1322,),  which  is  plainly  bedded.  a,nd  laminated,  and  dips  57" 
N.  W.,  the  strike  being  N.  47°  E. 

Southward  from  the  quartzite  outcrops  the  elevation  continues  to  be  between  500  and 
600  feet,  in  sections  23  and  26,  but  the  only  rock  to  be  seen  is  horizontal  sandstone. 
Westward  from  these  sections,  the  elevation  remains  about  the  same,  and  one  passes 


518  .     GEOLOGY  OF  CENTRAL  WISCONSIN. 

insensibly  on  to  the  Lower  Magnesian  limestone.  Eastward,  in  sections  24  and  25,  the 
descent  of  200  feet  to  the  headquarters  of  Seeley  creek  is  very  rapidly  made,  and  sand- 
stone is  exposed  through  nearly  the  whole  vertical  distance. 

On  Sec.  35,  a  large  exposure  of  reddish  glassy  quartzite  occurs  in  a  ravine,  at  an  ele- 
vation much  below  that  of  the  country  occupied  by  sandstone  to  the  northward.  A  few 
rods  up  the  ravine,  sandstone  ledges  occur  at  a  higher  level.  Taken  together  with  the 
construction  of  the  high  country  all  through  the  east  side  of  the  town  of  Wcstfield,  this 
outcrop  is  believed  to  indicate  the  existence  throughout  of  a  quartzite  core  only  slightly 
covered  with  sandstone  layers. 

The  outcrop  just  referred  to  is  on  the  slope  downward  towards  the  valley  of  the  Wis- 
consin, and  is  really  the  western  end  of  the  southern  quartzite  range.  From  here  east- 
ward to  Devil's  Lake,  we  find  this  range  as  bold  and  wide  as  it  is  east  of  the  lake,  and 
characterized  by  the  same  heavy  timber  and  clay  soil.  In  T.  10,  R.  5  E.,  Honey 
Creek,  the  southern  slope  of  the  range  is  in  the  northern  row  of  sections.  In  the  south 
side  of  T.  11,  R.  5  E.,  Freedom,  are  very  high  rounded  swells,  some  of  which  are 
amongst  the  highest  points  on  the  range.  On  the  northern  slope,  in  this  town,  the 
streams  flowing  north  into  the  Baraboo  set  back  into  the  ridge  in  deep  ravines,  about 
which  sandstone  sometimes  occurs  at  high  levels.  On  the  N.  W.  qr.  of  Sec.  22,  the 
quartzite  shows  in  two  bluffs,  150  feet  high,  on  either  side  of  the  creek,  with  a  distance 
between  of  about  one-eighth  of  a  mile.  The  rock  here  is  for  the  most  part  closely  like 
that  at  Devil's  Lake,  but  portions  are  unusually  light- colored  (1,271),  showing  a  light- 
brown  weathered  surface,  and  a  nearly  white,  slightly  granular,  fresh  fracture.  Regu- 
larly interbedded  is  a  soft,  light-gray,  greasy,  finely  laminated,  clay-plate  (1,272),  con- 
taining according  to  analysis  by  Mr.  A.  C.  Prescott:  silica,  59.84;  alumina  and  iron 
oxide,  35.39;  magnesia,  0.10;  water,  4.67  =  100;  the  iron  oxide  being  in  very  small 
amount  only.  Both  quartzite  and  slate  are  plainly  bedded,  the  strike  being  N.  23°  W., 
the  dip  16°  N. 

On  the  road  extending  southward  from  Bloom's  Station  across  the  range,  into  Honey 
creek,  horizontal  sandstone  ledges  are  seen,  as  far  as  the  N.  W.  qr,  of  Sec.  23,  at  an  ele- 
vation of  530  feet.  In  the  southern  part  of.  the  same  section,  quartzite  is  exposed  at  an 
elevation  of  700  feet,  and  along  the  east  side  of  Sec.  26,  an  elevation  of  830  feet  is 
reached. 

In  the  southern  row  of  sections  of  T.  11,  R.  6  E.,  Snmpter,  the  south  slope  of  the 
range,  is  very  bold  and  prominent,  owing  to  the  low  ground  of  Sauk  Prairie,  which 
stretches  from  the  foot  of  the  bluffs  for  eight  or  nine  miles  to  the  southward.  All  along 
the  slope  towards  the  prairie  are  large  rough  exposures,  —  as,  for  instance,  on  the  west 
Sauk  road  on  Sec.  34;  in  the  ravine  on  Sec.  27;  on  the  east  Sauk  road,  in  Sec.  35,  and 
all  along  the  range  eastward  from  here  to  the  Devil's  Nose.  On  the  north  slope  of  the 
range  in  the  N.  E.  qr.  of  Sec.  15,  T.  11,  R.  6  E.,  dark-grayish,  somewhat  granular 
quartzite  shows  in  a  large  exposure,  with  a  dip  of  26°  N. 

Within  the  circuit  of  the  quartzite  ranges,  are  a  few  isolated  points  of  quartzite 
and  schistose  rocks,  which  rise  through  the  sandstone  that  forms  the  basement  of  the 
valley.  One  of  these,  on  the  south  line  of  Sec.  29,  T.  12,  R.  7  E..  on  Peck's  Prairie,  is 
a  low  rounded  ridge  75  feet  high.  The  rock  here  (1,247)  is  a  light  pinkish-grey  meta- 
morphic  conglomerate,  composed  of  small  rounded  pebbles  of  quartzite  l-16th  to  l-8th 
inch  hi  diameter,  embedded  in  a  finer-grained  matrix  of  similar  character.  An  obscure 
N.  70°  dip  is  to  be  seen  at  a  few  points,  and  veins  of  milky  quartz  occur,  carrying  nests 
of  large-surfaced  brilliant  specular  iron  (1,248).  One  of  these  veins  is  75  feet  long  and 
2  feet  wide,  with  nests  and  seams  of  specular  iron,  1  to  3  inches  wide.  A  few  rods  west 
of  the  quartzite,  at  the  center  of  the  north  line  of  the  N.  W.  qr.  of  Sec.  32,  horizontal 
sandstone  ledges  are  seen. 

Other  areas  showing  quartzite  and  slate  occur  on  Sec.  5,  T.  11,  R.  6  E.;  Sec.  4,  T.  11 


THE  ARCILEAN  ROCKS.  519 

R.  5  E.;  and  Sec.  2,'T.  11,  R.  5  E.  The  two  former  are  high,  rocky  points,  the  latter 
a  low  outcrop  on  the  river  side.  Still  another  occurs  on  the  S.  E.  qr.  of  Sec.  33,  T.  12, 
R.  5  E.,  near  Ableman's.  Here  a  railway  cutting  passes  through  the  point  of  a  ridge, 
n^ar  the  north  bank  of  the  Baraboo  river.  At  tha  west  end  of  the  cutting  coarse  white 
sandstone,  in  horizontal  ledges,  lies  against  a  craggy  cliff  of  light-colored  quartz- schist 
(1284),  resembling  that  at  the  south  side  of  the  section  at  the  Lower  Narrows  of  the 
Baraboo  (see  Fig.  30),  but  less  regularly  slaty.  At  the  junction  of  the  two  rocks  large 
bowlders  of  quartzite  are  included  in  the  sandstone,  which  itself  fills  in  the  cracks  be- 
tween the  layers  of  schist.  One  hundred  and  thirty  feet  from  the  west  end  of  the  cut- 
ting, the  light-colored  schist  gives  place  to  a  gray  or  greenish  clayey  rock  (1283).  Some 
01  the  layers  are  bright  green  in  color,  and  marked  with  very  fine  lines  of  lamination. 
These  layers  are  apparently  quite  silicious.  Seventy  feet  further,  pinkish  granular 
quartzite  (1282)  is  indefinitely  exposed.  The  exposures  throughout  the  cutting,  though 
in  places  40  feet  high,  are  very  much  jointed  and  confused.  The  position  near  the  end 
of  the  ridge  has  caused  much  weathering  and  alteration.  There  is  evidently  a  high  dip, 
apparently  to  the  north. 

THE  MARCELLON  QUAKTZ-PORPHYKY. 

On  Sec.  7,  in  the  town  of  Marcellon,  Columbia  county,  on  each  side  of  the  road  in  the 
south  half  of  the  section,  are  two  low  rounded  hills,  40  to  60  feet  in  height,  of  quartz- 
porphyry  (759).  The  rock  exposures  are  large,  and  are  much  rounded  and  weather- 
worn, being  separated  into  numerous  bowlder-like  masses  by  wide-open,  earth-filled 
joints.  The  weathered  surfaces  have  a  prevailing  pinkish  tinge,  giving  the  idea  that 
the  rock  is  largely  composed  of  pink  felspar.  On  obtaining  a  fresh  fracture,  however, 
only  a  very  few,  sparsely  scattered,  minute  felspar  faces  are  to  be  seen,  the  mass  of  the 
rock  being  composed  of  a  brownish  to  blackish  compact  matrix.  Two  general  varieties 
occur,  one  presenting  a  light  brownish  color,  showing  a  tendency  to  flake  off  in  frag- 
ments that  are  translucent  on  the  edges,  and  containing  no  distinguishable  felspar 
crystals,  the  other  having  a  dark-gray  to  black  matrix,  in  which  are  to  be  seen  a  few 
distinct  crystals  of  felspar  and  numerous  copper-colored  points  of  iron-sesquioxide.  The 
rock  has  nearly  the  hardness  of  quartz,  and  fuses  only  with  the  greatest  difficulty.  A 
more  silicious  character  as  compared  with  other  quartz-porphyries  of  the  state  is  thus  in- 
dicated, and  the  indication  is  borne  out  by  the  content  of  silica  —  76.98  per  cent.  —  as 
shown  by  analysis.  We  have  evidently,  in  this  case,  a  porphyry  which,  in  its  large 
content  of  silica,  and  in  the  sparseness  of  its  felspar  crystals,  approaches  the  true  felsites 
(petrosilex,  halleflinta).  Quite  a  distinct  and  uniform  set  of  bedding  joints  occurs,  the 
strike  being  N.  32°  E.,  the  dip  65°  to  75°  N.  W.  Numerous  cross-joints  traverse  the 
rock,  and,  on  weathered  portions,  cause  it  to  fly  into  smooth-faced,  angular  fragments, 
at  the  least  blow  of  the  hammer.  The  surrounding  country  is  occupied  by  the  Potsdam 
sandstone,  which  is  exposed  at  many  points. 

THE  OBSERVATORY  HILL  QUARTZ-PORPHYRY. 

Six  miles  north  of  the  Marcellon  outcrop,  in  the  S.  E.  qr.  of  Sec.  7,  in  the  town  of 
Buffalo,  Marquette  county,  a  knob  of  quartz-porphyry  rises  250  feet  above  the  general 
level,  and  490  feet  above  Lake  Michigan.  On  the  flanks  of  the  hill  and  up  to  a  vertical 
distance  above  the  base  of  125  feet,  are  horizontal  sandstone  ledges.  Above,  to  the 
top,  are  nearly  continuous  outcrops  of  porphyry,  with  a  not  very  plain  N.  32°  E.  strike, 
and  60°  N.  W.  dip.  These  bedding  directions  are  the  same  as  on  the  Marcellon  out- 
crop. 

The  porphyry  (762)  has  a  dark-grayish  to  black  compact  matrix,  in  which  are  thickly 
scattered  quite  large  (one-eighth  to  one-fourth  inch  in  diameter)  brownish  to  pink  facet*. 


520  GEOLOGY  OF  CENTRAL  WISCONSIN. 

r,f  felspar,  the  whole  presenting  a  veiy  dark- colored  appearance.  The  silica  content  is 
73.56  per  cent.,  and  the  specific  gravity,  2.60.  Numerous  close  joints  occur  throughout 
the  exposure,  causing  the  rock  to  split  like  that  of  the  Marcellon  outcrop  into  small,  ir- 
regularly shaped,  smooth-faced,  angular  fragments. 

The  surrounding  country  shows  everywhere  the  Potsdam  sandstone  as  the  surface 
rock.  A  high  bluff  of  this  sandstone,  some  100  feet  lower  than  the  top  of  the  Observa- 
tory, lies  on  the  S.  W.  qr.  of  the  same  section. 

THE  MOUND VILLE  QUARTZ-POBPHYRY. 

On  the  edge  of  the  Fox  river  marsh  at  the  head  of  Lake  Buffalo,  on  the  line  between 
sections  8  and  5,  T.  14,  R.  9  E.,  Moundville,  Marquette  county,  are -three  low  rounded 
outcrops  of  quartz-porphyry.  These  are  five  miles,  in  a  direction  10°  N.  of  W.,  from 
Observatory  Hill,  which  is  the  nearest  Archaean  outcrop.  No  other  rock  shows  in  the 
neighborhood,  the  country  being  heavily  drift-covered.  The  largest  outcrop  is  on  the 
east  end  of  a  low  bluff  35  feet  high,  and  several  hundred  feet  in  length.  There  are 
quite  marked  appearances  here  of  the  same  N.  E.  strike,  and  N.  60°  dip,  as  seen  at 
Observatory  Hill  and  in  Marcellon.  The  rock  (1430)  has  a  dark  brown  matrix,  re- 
sembling in  this  regard  the  Marcellon  porphyry,  from  which  it  differs,  however,  in  show- 
ing throughout  traces  of  crystalline  structure,  and  quite  thickly  scattered,  large,  brown- 
ish felspar  surfaces.  A  few  crystals  are  white  and  translucent.  The  weathered  sur- 
face is  often  of  a  bnght  pink  color.  Mr.  Wright's  microscopic  examination  (Appendix) 
shows  that  fine  magnetite  particles  are  abundant.  Their  existence  is  not  rendered  evi- 
dent even  by  the  us"e  of  the  ordinary  lens.  The  silica  content  is  72.76  per  cent. 

THE  SENECA  (PiNE  BLUFF)  QUAKTZ-PORPHYEY. 

A  rounded  elliptical  knob  of  quartz-porphyry,  100  feet  high,  %ih  mile  long,  and  >^th 
mile  wide,  lies  on  the  north  side  of  the  White  river  marsh,  in  Sec.  2,.  T.  17,  R.  11  E., 
Seneca,  Green  Lake  county.  The  greatest  extension  of  the  hill  is  in  an  east  and  west 
direction.  It  is  largely  rocky,  but  there  are  no  abrupt  rock  ledges,  the  exposures  being 
almost  entirely  surfaces  conforming  to  the  general  contour  of  the  hill,  and  on  a  level 
with  the  surrounding  sod.  In  places,  the  slopes  of  the  hill  are  covered  with  angular 
fragments,  apparently  split  off  by  frost.  This  is  a  peculiarity  not  noticed  on  any. of  the 
other  porphyry  outcrops,  ar,d  appears  to  be  due  to  the  large  content  of  comparatively 
coarse,  cleavable  felspar.  The  hill  is  only  about  two  miles  south  from  the  granite  hills 
of  Spring  Lake,  in  T.  18,  R.  11  E.,  Waushara  county.  The  surrounding  country  is 
marshy  and  drift-covered,  and  shows  no  outcrop  of  horizontal  rocks.  The  loose  frag- 
ments are  many  of  them  smoothed  on  one  side,  and  some  surfaces  are  most  beautifully 
striated.  Owing  to  the  broken  condition  of  the  outcrop,  no  definite  bedding  planes  were 
made  out,  though  weathered  specimens  brought  away  show  distinct  traces  of  lamination. 

This  porphyry  in  its  least  weathered  portions  (1410)  shows  a  light-gray  to  whitish  fine- 
grained matrix,  made  up  largely  of  fine  glassy  felspar 'Crystals,  and  containing  numer- 
ous large  surfaces  of  the  same  kind.  The  more  weathered  specimens  (1412)  have  a  pink 
to  white,  quite  distinctly  granular  matrix,  in  which  with  the  lens  can  be  seen  what  ap- 
pear to  be  angular  grains  of  quartz.  The  glassy  felspar  crystals  are  also  abundant. 
The  weathered  surface  is  brownish,  with  a  kaolinized  undercrust.  Nearly  all  of  the  rock 
shows  signs  of  weathering.  The  silica  content  is  76.39  per  cent. 

THE  MAEQUETTE  AND  BERLIN  QUAETZ-PORPHYEIES. 

The  large  outcrops  of  quartz-porphyry  on  sections  34  and  35,  T.  15,  R.  11  E.,  and  sec- 
tions 2  and  3,  T.  14,  R.  11  E.,  near  the  village  of  Marquette,  Green  Lake  county,  were 


THE  ARCH^AN  ROCKS.  521 

originally  regarded  as  within  the  Central  Wisconsin  district,  of  which,  however,  by  sub- 
sequent agreement,  the  Fox  river  was  made  the  southern  boundary.  They  will,  there- 
fore, be  described  by  Prof.  Chamberlin,  in  whose  district  is  also  the  outcrop  at  the  city 
of  Berlin,  Green  Lake  county.  As  the  writer  has  examined  both  localities  carefully,  he 
may  be  permitted  to  allude  to  the  nature  of  the  rock  of  each,  for  the  sake  of  comparison 
In  the  Marquette  outcrops,  the  prevailing  rock  (761,  1,426),  noticed,  has  a  black,  com- 
pact, flinty  matrix,  which  is  streaked  with  white  non-continuous  lines.  These  lines  are, 
for  the  most  part,  very  prominent,  and  are  frequently  much  contorted,  the  whole  rock 
having  a  very  evident  parallel  grain.  The  felapar  crystals  are  minute  and  sparse.  The 
silica  content  (1,426),  is  70.29  per  cent,  less  than  obtained  from  any  other  of  the  Wis- 
consin porphyries.  The  general  course  of  the  contorted  laminse  points  to  the  same 
N.  E.  strike  direction,  as  observed  on  the  Marcellon,  Observatory  Hill,  and  Moundville 
outcrops. 

The  Berlin  rock  has  a  dark  bluish-gray  matrix,  much  streaked  with  white,  and  hav- 
ing a  peculiar  fine-granular,  quartz-like  texture,  as  seen  under  the  lens.  The  felspar 
crystals  are  small,  greyish  to  brownish,  and  rather  numerous.  The  lamination  is  very 
fine  and  distinct,  and  often  contorted,  and  the  silica  content  74.37  per  cent. 

A  comparison  of  the  rocks  of  the  several  porphyry  areas  shows 
that  though  all  present  the  same  general  kind  of  rock,  no  two  of  the 
areas  are  exactly  alike  in  this  regard.     The  porphyry  associated  with 
the  Baraboo  quartzite  has  a  dark  brown   to  black  matrix,  numerous 
large,  pink,  felspar  crystals,  and  71.24  per  cent,  of  silica.     The  Mar- 
cellon porphyry  has  a  brown  to  black  matrix,  is  almost  without  felspar 
facets,  and  contains  77  per  cent,  of  silica.     The  Observatory  Hill  por- 
phyry has  a  black,  flinty  matrix  with  numerous  large,  brownish  felspar 
facets,  and  contains  73.56  per  cent,  of  silica.    The  Moundville  porphyry 
resembles  the  Marcellon  rock  in  the  color  and  appearance  of  the  matrix, 
but  contains  much  brownish  felspar,  some  magnetite,  and  only  72.76 
per  cent,  of  silica.     The  Seneca  porphyry  is  altogether  different  from 
the  others,  in  having  a  light  colored,  nearly  white,  somewhat  granular, 
and  distinctly  quartzose  matrix,  and  in  containing  much  white,  glassy 
felspar,  the  percentage  of  silica  being  76.39.    The  Marquette  porphyry 
has  a  black,  flinty  matrix,  in  this  regard  resembling  closely  the  Obser- 
vatory Hill  rock,  from  which,  however,  it  differs  in  being  almost  with- 
out felspar  facets  and  in  having  its  matrix  streaked  with  white,  and 
thus  presenting  a  very  marked  lamination,  the  silica  content  being  70.29, 
or  less  than  that  obtained  from  any  other  of  these  rocks.     The  Berlin 
porphyry  resembles  that  from  the  Marquette  outcrop  in  having  a 
marked  lamination,  but  differs  in  the  color  of  its  matrix,  in  contain- 
ing plentiful  felspar  facets,  and  in  having  a  larger  percentage  (74.37) 
of  silica.     Its  peculiar  fine  granular  matrix  is  also  a  very  distinguish- 
ing characteristic. 

THE  MONTELLO  GEANITE. 

In  the  village  of  Montello,  on  the  west  side  of  Sec.  9,  T.  15,  R.  10  E.,  Marquette 
county,  is  an  elliptical- shaped  rounded  mound  of  pink  granite,  about  a  third  of  a  mile 


522  GEOLOGY    OF   CENTRAL  WISCONSIN. 

in  length,  and  40  feet  high.  Over  most  of  the  hill  the.  rock  (756,  758,  764,  765)  is  quite 
uniform  on  a  fresh  fracture,  though  presenting  a  weathered  surface:  from  bright  pink  to 
dull  grayish-pink  in  color.  The  weathering  is  very  slight,  however,  and  the  rock  shows 
almost  no  tendency  to  decompose.  It  has  a  medium  grain,  close  texture,  is  of  a  bright 
pinkish  color,  and  without  sign  of  arrangement  of  the  ingredients  in  lines.  These  are: 
rather  large-flaked,  pinkish,  cleavable  felspar,  predominating;  somewhat  granular, 
fine,  pinkish,  translucent  quartz,  abundant;  and  greenish-black  mica,  sparsely  scattered, 
in  blotches  made  up  of  very  fine  flakes.  In  places,  thin  light- green  epidote-colored 
seams  occur  (757).  Somewhat  irregular  N.  W.  joints  traverse  the  rock  which  is,  how- 
ever, for  the  most  part  structureless,  and  is  quarried  by  firing,  the  pieces  that  crack  off 
presenting  a  conchoidal  fracture.  On  the  north  side  of  the  west  end  of  the  mound  oc- 
curs a  vertical  layer  (or  vein?)  three  feet  wide,  trending  N.  55°  E.,  of  a  soft  greenish, 
highly  schistose,  decomposing  chloritic  rock  (758).  The  least  weathered  specimens  show 
a  blackish  color  and  some  tendency  to  a  crystalline  texture.  The  vein  is  weathered 
down  for  two  or  three  feet  below  the  enclosing  granite  walls,  both  of  which  are  seen. 
The  schistose  laminae  are  parallel  to  the  walls.  Greenish  epidote  seams  in  the  rock  near 
by  have  the  same  trend  as  the  vein.  Though  this  granite  might  be  somewhat  difficult 
to  obtain  in  dressable  masses,  it  would  undoubtedly  make  a  very  handsome  and  durable 
stone. 

THE  MARION  GRANITE  AREAS. 

In  the  the  town  of  Marion,  T.  18,  R.  11  E.  Waushara  county,  are  three  low  granite 
knobs.  Two  of  these.  Stone  and  Pine  Bluffs,  are  on  the  N.  E.  qr.  Sec.  27,  about  two 
miles  in  a  N.  N.  W.  direction  from  the  quartz-porphyry  hill  of  the  town  of  Seneca, 
Green  Lake  county;  and  the  third,  a  larger  and  bolder  hill,  lies  on  the  eastern  border 
of  the  marsh,  on  Sees.  12  and  13,  and  stretches  to  some  extent  over  the  line  into  the 
town  of  Wan-en,  On  all  of  these  areas  the  rock  (766,  Sec.  27;  767,  768,  Sec.  12)  ob- 
served is  nearly  the  same,  a  pinkish  felspathic  granite,  mottled  with  gray  and  green, 
closely  resembling  the  Montello  granite,  from  which  it  differs,  however,  in  having  a 
coarser  grain,  less  close  texture,  and  a  marked  tendency  to  decompose.  Reddish  cleav- 
able felspar  is  the  principal  ingredient,  occurring  in  facets  up  to  %th  and  j^th  inch  in 
diameter;  quartz  is  abundant,  fine-granular  and  translucent;  mica  is  sparse,  and 
scattered  in  small,  greenish-black  blotches.  Large  whitish  porphyritic  felspar  occurs. 
There  is  no  sign  of  any  arrangement  of  the  ingredients,  or  of  any  parallel  grain  to  tha 
rock.  No  definite  bedding  planes  were  observed  on  any  of  the  outcrops,  though  numer- 
ous crossing  joint  planes  occur,  and  quite  regular  flat  slabs  are  sometimes  obtainable. 
Veins  of  white  quartz  occur.  The  most  marked  characteristic  of  the  rock  is  its  tendency 
to  weather  and  shell  off  in  crumbling  masses.  Some  of  the  large  flat  surfaces  are  so  far 
crumbled  as  to  be  penetrated  readily  by  a  horse's  hoof.  The  rock  from  these  outcrops 
would  polish  easily,  but  its  tendency  to  crumble  renders  it  less  valuable  than  the  Mon- 
tello granite. 

Conclusions.  As  indicated  by  their  common  character  and  strike 
direction,  as  well  as  their  relative  positions,  the  quartz-porphyry  and 
granite  patches  of  Columbia,  Marqnette,  Green  Lake  and  Waushara 
counties,  which  have  been  described  in  the  foregoing  pages,  are  doubt- 
less to  be  regarded  as  but  projecting  points  of  one  northeastward 
trending  belt,  the  rest  of  which  is  buried  beneath  the  Silurian  sand- 
stone and  later  superficial  deposits.  All,  both  granites  and.  porphy- 
ries, belong  evidently  to  the 'same  formation.  Moreover,  the  occur- 


THE  ARCILEAN  ROCKS.  523 

rence  of  similar  porphyry  with  the  quartzites  of  the  Baraboo 
ranges,  throws  all  the  areas,  without  question,  into  the  same  category 
as  those  qnartzites.  We  have  thus  a  great  quartzite  series,  including, 
also,  quartz-porphyries,  and  associated  with  these  pinkish,  close-tex- 
tured, (intrusive?)  granite.  Such  an  association  is  not  a  new  one. 

Percival l  in  alluding  very  briefly  to  some  of  the  porphyry  and 
granite  areas,  the  rocks  of  which,  however,  he  calls  by  other  and  in- 
correct names,  intimates  that  the  granite  patches  (his  syenite)  form  a 
belt  altogether  to  the  westward  of  the  others.  This  conclusion  is  not 
borne  out  by  the  facts.  The  Moundville  porphyry  lies  on  a  line,  as 
indicated  by  the  1ST.  32°  E.  strike,  altogether  west  of  the  Montello  and 
Marion  granites,  which  are  thus,  evidently,  but  portions  of  the  same 
series. 

The  entire  width  of  the  granite  and  porphyry  belt,  at  right  angles 
to  the  trend,  is  not  less  than  twenty-five  miles,  the  Mackford  area  ly- 
ing on  the  extreme 'east,  that  of  Montello  on  the  extreme  west.  The 
length  from  the  Marcellon  area  on  the  south,  in  a  N.  32°  E.  direction, 
is  30  miles.  Regarding  the  belt  as  continuous,  as  it  undoubtedly  is, 
with  the  Baraboo  ranges,  it  is  evident  that  it  must  make  a  great  bend 
northeastward,  in  the  region  about  Portage.  A  glance  at  Plate 
XVIII  of  this  volume,  will  suffice  to  show  that,  towards  their  eastern 
ends,  the  quartzite  ranges  are  already  on  the  turn. 

The  parallelism  of  the  belt  thus  made  out  with  the  edge  of  the 
main  Archaean  area  to  the  northward,  is  striking,  and  strongly  sug- 
gests that  we  have  here  part  of  a  once  continuous  band  of  Huronian 
surrounding  the  old  northern  core,  after  the  manner  of  the  later  Silu- 
rian formations. 

THE  NECEDAH  QUARTZITE. 

Dotting  the  great  sand  plain  of  the  Wisconsin  in  Juneau  and  Adams  counties,  are 
numerous  bold  castellated  outliers  of  the  Potsdam  sandstone,  rising  abruptly  from  the 
plain,  and  constituting  very  marked  features  of  the  scenery.  From  the  same  plain,  and 
only  about  three  miles  west  from  one  of  the  greatest  of  the  sandstone  bluffs  —  Petenwell 
Peak  —  rises  the  quartzite  hill  at  the  foot  of  which  the  village  of  Necedah  is  built.  The 
rounded  contour  of  this  hill  serves  to  mark  it  at  once  as  different  in  nature  from  the 
sandstone  bluffs  of  the  adjoining  region. 

The  main  Necedah  bluff  lies  on  the  N.  W.  qr.  of  Sec.  25,  T.  18,  R.  3  E.,  the  town 
line  crossing  over  its  eastern  end;  it  is  about  half  a  mile  in  length,  with  its  greatest  ex- 
tension east  and  west,  and  is  highest,  and  at  the  same  time  most  bold  and  rocky,  on  its 
eastern  end,  which  rises  170  feet  above  the  street  below,  and  about  510  feet  above  Lake 
Michigan.  A  short  distance  southeast  of  the  main  bluff,  on  the  N.  W.  qr.  of  the  S.  W. 
qr.  of  Sec.  19,  T.  18,  R.  4  E.,  is  a  small,  craggy  hill,  75  feet  high,  of  the  same  rock  as 
that  composing  the  main  hill,  the  intervening  low  ground  being  underlaid  by  horizontal 
sandstone. 

.!  Annual  Report  of  Geological  Survey  of  Wisconsin  for  1855,  p.  105. 


524  GEOLOGY  OF  CENTRAL  WISCONSIN. 

The  exposures  on  the  main  hill  are  mostly  on  the  eastern  and  southeastern  portions 
where  in  places  they  rise  nearly  precipitously  from  the  low  ground  at  foot.  The  rock 
seen  here  is  for  the  most  part  (1354)  a  glassy,  translucent,  subgranular,  grayish  quartz  - 
ite,  much  more  nearly  allied  to  the  quartzite  of  Rib  and  Mosinee  hills  in  Marathon 
county,  than  to  that  of  the  Baraboo  ranges.  Much  of  the  rock  is  quite  dark-gray  in 
color,  the  quartz  then  being  still  glassy  but  smoky-tinted.  Numerous  small  cavities 
and  seams  occur,  lined  with  half  crystalline  quartz,  and  carrying  a  soft,  pinkish,  clayey 
substance;  bluish-white  quartz  veins  (1355*2)  one-half  to  two  inches  in  width,  and 
nests,  are  also  common,  and  these  carry  frequently  fine-flaked,  brilliant,  .specular  iron, 
which  occurs  also  occasionally  in  quite  large  masses,  similar  to  those  found  in  the  Bara- 
boo quartzite.  No  parallel  grain  is  to  be  seen  in  this  rock,  nor  any  definite  bedding 
planes.  Numerous  quite  close  joints  occur,  however,  and  these  cause  the  rock  to  weath- 
er into  smooth-faced,  sharp- angled  fragments.  On  the  smaller  bluff  a  very  distinct 
parallel  grain  is  to  be  seen  trending  N.  75°  W.,  and  showing  a  corresponding  dip  of 
45°  N.  Here  much  of  the  quartzite  is  of  a  light  pink  color,  looking,  on  a  fresh  fracture, 
almost  like  a  fine-grained,  pinkish  granite  (1358;,  but  the  only  prominent  mineral  is  sub- 
granular,  translucent,  pinkish  quartz.  Some  specimens  show  mica  plainly  in  very 
sparsely  scattered,  small  scales.  In  many  places  little  centers  of  iron-staining  seem  to 
be  decomposing  mica  scales.  Other  portions  of  this  rock  (1358,  1357)  are  opaque,  white, 
and  distinctly  granular,  and  are  seamed  with  fine  black  lines,  arranged  so  as  to  show 
discordant  stratification.  These  seams  when  split  open,  appear  to  be  composed  of 
blackish  mica.  Bluish- white  veins  and  nests  occur  here  also. 


.'• 


( ' 


v. 


TllF.  M1IA,«.KliP.!,,THO.«r  K»,,K  Co 

POTSDAM  SANDSTONE:, 

-Southern-  end  of  Roche  a  (Vis  Bluff,  Adams  Co.  £25  ft .  hi  gh. 


THE  LOWER  SILURIAN  ROCKS.  525 


CHAPTER   IT. 
THE   LOWER   SILURIAN   ROCKS. 

I.  In  General. 

THE  LOWER,  OR  POTSDAM,  SANDSTONE  SERIES. 

Forming  the  base  of  the  pile  of  Silurian  strata  everywhere  in  the 
states  bordering  the  Upper  Mississippi,  but  having  a  much  greater 
surface  development  in  Wisconsin  than  elsewhere,  and  resting  di- 
rectly upon  the  irregular  surface  and  upturned  edges  of  the  older 
crystalline  rocks,  is  a  great  thickness  of  sandstone,  which,  through  the 
larger  part  of  its  mass,  is  made  up  of  rolled  grains  of  quartz,  of  vary- 
ing size,  cemented  together  by  a  minute  quantity  of  hydrous  iron 
oxide.  Towards  the  upper  part  of  the  formation,  in  Central  Wiscon- 
sin, this  sand  becomes  mingled  with  more  or  less  dolomitic  and  cal- 
careous material,  which  further  up  tends  to  aggregate  into  thin  bands 
of  limestone,  finally  forming,  at  35  to  50  feet  below  the  base  of  the 
next  great  formation,  the  Lower  Magnesian  limestone,  a  well  marked 
and  very  persistent  yellow  limestone  layer,  which  has  a  thickness  of 
30  feet,  and  is  so  well  marked  and  important  a  horizon  in  Central 
Wisconsin,  that  I  have  given  it  the  specific  name  of  Mendota  lime- 
stone, from  a  large  exposure  at  MacBride's  point  on  the  north  shore 
of  lake  Mendota.  Above  the  Mendota  horizon,  sandstone,  35  to  50  feet 
in  thickness,  again  comes  in,  the  larger  part  of  which  is  either  nearly 
pure  white  quartz  sand,  or  sand  turned  brown  by  oxide  of  iron,  thus 
approaching  more  nearly  in  character  to  the  Upper  or  St.  Peters 
sandstone  than  to  that  immediately  beneath  the  Mendota  beds.  To- 
wards its  upper  portions,  however,  just  beneath  the  overlying  lime- 
stone, it  generally  becomes  again  somewhat  dolomitic,  the  upper  limit 
being  frequently  marked  by  layers  of  greensand  and  oolitic  chert. 
To  this  layer  I  have  given  the  name  of  Madison  sandstone,  it  yield- 
ing large  quantities  of  a  very  excellent  building  sandstone  at  Madi- 
son. These  names  are  not  meant  to  be  of  anything  more  than  local 
importance. 

For  some  distance  above  the  Madison  horizon  the  Lower  Magnesian 


526  GEOLOGY  OF  CENTRAL  WISCONSIN. 

itself  often  shows  alternations  of  nearly  purely  dolomitic,  and  distinctly 
sandy  layers,  even  including  thin  seams  of  white  sand,  whilst  some 
sandy  material  occurs  at  horizons  well  towards  the  summit  of  this  for- 
mation. The  two  series  thus  evidently  graduate  into  one  another, 
and  in  many  parts  of  the  northwest  it  is  undoubtedly  difficult  to  fix 
upon  the  dividing  line.  In  Central  Wisconsin,  however,  the  alter- 
nating beds  are  well  defined,  and  two  horizons  are  well  marked  by 
beds  of  greensand.  These  are  the  base  of  the  Lower  Magnesian  prop- 
er, and  the  base  of  the  Mendota  beds,  65  to  100  feet  below.  During 
the  writer's  earlier  work  in  this  field,  the  lower  of  these  limits  was 
adopted,  in.  mapping,  as  the  line  of  division  between  the  two  forma- 
tions, whilst  subsequently  both  horizons  were  mapped,  the  upper  one 
being  taken  as  the  base  of  the  Lower  Magnesian,  in  order  that  that 
name  might  cover  the  same  beds  as  included  under  it  by  other  mem- 
bers of  the  geological  corps. 

The  facts  which  led  at  first  to  the  use  of  the  lower  limit  may  be 
briefly  given  here.  In  Dane  and  Columbia  counties,  where  the  Men- 
dota and  Madison  horizons  are  very  prominent,  and  were  first  made 
out,  the  entire  thickness  of  the  Lower  Magnesian,  between  the  upper 
surface  of  the  Madison  beds  and  the  base  of  the  St.  Peters  or  Upper 
sandstone,  was  found  to  be  only  50  to  80  feet.  It  Avas  well  known 
that  not  far  to  the  westward,  along  the  Wisconsin,  this  formation 
attains  a  thickness  of  250  feet.  It  was  not  thought  so  great  a  thick- 
ening as  this  could  exist,  and  to  explain  the  difference,  it  was  supposed 
that  the  Mendota  and  Madison  beds  were  a  local  modification  of  the 
lower  portion  of  the  Lower  Magnesian  formation.  This  supposition 
was  encouraged  by  the  great  similarity  between  the  Mendota,  as  seen 
in  the  typical  localities  in  Dane  .county,  and  the  limestone  beds  im- 
mediately overlying  the  Madison  sandstone,  the  former  here  being  al- 
most a  pure  dolomite,  with  only  two  or  three  percent,  of  insoluble  resi- 
due. Subsequently,  however,  it  was  ascertained  beyond  a  doubt  that  the 
Mendota  beds  are  to  be  recognized  occupying  the  same  position  below 
the  Lower  Magnesian,  even  where  that  formation  attains  its  greatest 
thickness,  its  irregularity  in  this  regard  being  proved  to  be  due  to  its 
having  suffered  a  surface  erosion  prior  to  the  deposition  upon  it  of  the 
St.  Peters  sandstone.  The  Madison  and  Mendota  beds  were  therefore 
thrown  back  into  the  Potsdam  series  as  its  uppermost  layers,  and  are 
so  mapped  on  all  of  the  Atlas  maps. 

For  all  those  portions  of  the  maps,  however,  which  represent  the 
Central  Wisconsin  district,  except  southwestern  Juneau  county,  on 
Area  II,  the  base  of  the  Mendota  beds  is  indicated  by  a  brown  line 
within  the  color  for  the  Potsdam  series,  the  space  between  this  line 


THE  LOWER  SILURIAN  ROCKS.  527 

and  the  brown-colored  Lower  Magnesian  area  being  occupied  by  the 
Madison  and  Mendota  beds.  In  the  sections  also,  both  of  the  Atlas 
plates  and  of  the  plates  in  this  volume,  the  Mendota  and  Madison 
beds  are  given  separately  from  the  Potsdam.  Having  been  mapped 
out  with  some  care,  it  was  thought  best  not  to  lose  the  work  done  on 
them  by  not  so  distinguishing  them.  Moreover,  the  close  likeness 
often  borne  by  the  Mendota  to  the  Lower  Magnesian,  and  the  gradu- 
ation of  one  series  into  the  other,  render  it  a  matter  of  doubt  whether 
to  affiliate  these  beds  of  passage  with  the  upper  or  lower  of  the  two 
series.  Constituting  so  important  a  feature  as  they  do  in  the  Central 
Wisconsin  stratigraphy,  they  deserve  separate  mention;  they  are 
really  beds  of  passage,  and  as  such  are  separately  considered  below. 
The  term  Potsdam,  then,  as  used  in  the  detailed  descriptions  and  sec- 
tions of  this  chapter,  applies  only  to  those  beds  terminating  upwards 
at  the  Mendota  base. 

Of  the  two  names  given  to  the  series  the  term  "  Lower  Sand- 
stone" was  used  by  Dr.  D.  D.  Owen,  as  distinguishing  it  from  an- 
other much  thinner,  but  very  prominent,  sandstone,  which  overlies 
the  Lower  Magnesian  —  the  Upper  or  St.  Peters  sandstone.  Hall  and 
Whitney  first  used  the  term  "Potsdam,'*  transferring  it  from  the 
sandstone  series  which  .forms  the  Silurian  base  in  the  state  of  New 
York,  and  contains  a  few  fossils  close  to  those  in  the  Wisconsin  beds, 
which,  however,  contain  many  that  are  not  found  in  New  York. 
That  the  two  formations  are  somewhere  nearly  the  equivalents  of  one 
another  appears  evident,  as  Hall  has  shown.1  The  extension  of  the 
New  York  name,  originally  given  to  a  comparatively  small  thickness 
of  rock  which  occupies  a  restricted  area,  to  the  lowest  of  the  fossil- 
iferous  Silurian  beds  all  over  the  country,  seems,  however,  unfortunate, 
and  especially  so  in  the  case  of  the  Wisconsin  formation,  which  has 
a  thickness  of  800  to  1,000  feet,  comes  to  the  surface  over  an  extended 
area,  and  is  far  more  fossiliferous  than  the  New  York  beds. 

Of  former  investigations  on  the  Potsdam  series,  Dr.  Owen's  seem 
to  have  been  much  the  most  exhaustive.  He  presents  a  scheme  of 
the  subordinate  structure  of  the  formation  which  may  be  considered 
quite  remarkable  for  so  early  a  day.  His  detailed  investigations, 
however,  did  not  extend  far  away  from  each  side  of  the  Mississippi, 
and  the  great  central  area  of  Wisconsin,  where  the  formation  spreads 
over  a  district  100  miles  in  diameter,  and  presents  elements  of  strat- 
ification contrasting  much  with  those  exhibited  along  the  Mississippi, 
he  left  hardly  touched.  Having  no  data  from  Artesian  borings,  he 
greatly  underestimated  the  thickness  of  the  formation,  putting  it  at 

1 16th  Annual  Report  N.  Y.  State  Cabinet  Natural  History. 


528  GEOLOGY  OF  CENTRAL  WISCONSIN. 

500  feet  as  an  extreme,  instead  of  800  to  1,000  feet.  Into  this  error 
lie  appears  to  have  been  led  by  committing  the  graver  one  of  sup- 
posing that  he  had  to  do  with  the  base  of  the  sandstone  whenever  he 
found  it  in  contact  with  the  crystalline  rocks,  losing  sight  altogether 
of  the  great  irregularities  of  the  upper  surface  of  the  latter  rocks,  by 
virtue  of  which  they  rise  high  into  the  upper  parts  of  the  sandstone 
series.  In  cases  like  that  exhibited  at  the  Dalles  of  the  St.  Croix, 
where  the  Copper-bearing  rocks  are  seen  to  rise  nearly  perpendicularly 
through  many  feet  of  the  sandstone,  he  regarded  the  traversing  rock 
as  "  intrusive,"  or  of  later  origin  altogether. 

Hall's  investigations  in  the  Central  Wisconsin  region  do  not  ap- 
pear to  have  been  any  more  extensive  than  those  of  Dr.  Owen,  to 
whose  descriptions  of  the  stratigraphy  of  the  series  he  adds  little  that 
is  new.  As  regards  the  fossils  of  the  formation,  however,  he  makes 
a  very  important  contribution,1  giving  a  list  to  which  little  has  been 
added  by  the  present  survey,  as  far  as  Central  Wisconsin  is  concerned, 
and  a  grouping  of  the  fossils  into  those  characterizing  the  lower,  mid- 
dle and  upper  beds,  which,  in  its  general  order,  proves  to  be  quite  cor- 
rect. He  commits  the  same  error  as  Dr.  Owen,  however,  with  regard 
to  the  thickness  of  the  formation,  placing  it  at  only  500  feet.2  As  a 
result  of  this,  his  list  of  fossils  from  the  lower  beds  must  be  assigned 
to  about  the  middle  of  the  series,  below  which  are  full  500  feet,  about 
whose  fossils,  or  lack  of  fossils,  we  know  nothing  at  all.  This  may  be 
regarded  as  a  point  of  some  importance  in  comparing  the  Wisconsin 
Primordial  with  that  of  other  regions  by  the  fossils  contained.  Whit- 
ney, who  reports  on  the  Lead  Region  in  Hall's  volume  on  Wisconsin 
Geology,  follows  the  latter  gentleman  in  his  under-estimate  of  the 
thickness  of  the  Potsdam  series. 

Of  all  of  the  earlier  accounts  of  the  geology  of  Central  Wisconsin, 
I  have  found  that  of  Dr.  Percival,  who  worked  after  Owen  and  before 
Hall  and  Whitney,  by  far  the  most  reliable.  Dr.  Percival  published 
two  small  annual  reports,  in  pamphlet  form,  whilst  geologist  of  the 
state,  in  both  of  which  he  gives  descriptions  of  the  Wisconsin  forma- 
mations,  whilst  one  of  the  two  gives  an  account  of  a  reconnoisance  in 
the  Potsdam  sandstone  region  of  the  heart  of  the  state.  He  recog- 
nizes distinctly  the  very  great  thickness  of  the  formation,  its  lack  of 
uniform  character,  and  the  fact  that  much  confusion  had  been  caused 
by  the  reference  to  the  Lower  Magnesian,by  Dr.  Owen  and  his  assist- 
ants, of  several  distinct  limestone  bands  separated  by  sandstone  strata, 
and  regarded  by  Percival  as  included  in  the  Lower  sandstone,  this 

1 16th  An.  Rep.  N.  Y.  State  Cabinet  of  Kat.  Hist. 
a  Report  on  the  Geology  of  Wisconsin,  Albany,  1862,  p.  16. 


THE  LOWER  SILURIAN  ROCKS.  529 

applying  especially  to  the  succession  of  strata  exposed  along  the  St. 
Croix  river.  He  notices  also,  distinctly,  the  bed  I  have  called  the  Men- 
dota,  and  also  numbers  of  other  minor  points  mentioned  by  no  other 
geologist. 

The  surface  distribution  of  the  Lower  Sandstone  exceeds  that  of 
any  other  of  the  formations  of  the  Central  Wisconsin  district.  The 
region  occupied  by  it  embraces  all  of  Juneau,  Adams,  "Waushara  and 
Marquette  counties,  as  also  more  or  less  of  Portage,  Wood,  Clark, 
Jackson,  Sauk,  Green  Lake,  Columbia  and  Dane  counties  —  in  all,  an 
area  of  over  6,000  square  miles.  The  total  area  occupied  by  the  for- 
mation outside  the  Central  Wisconsin  district,  and  within  the  state, 
is  probably  as  large  again,  but  nowhere  else  is  there  one  continuous 
area  of  so  great  diameter  as  in  the  central  counties.  Over  a  large 
portion  of  this  district,  in  Jackson,  Wood,  Clark,  Portage,  and  por- 
tions of  Juneau  and  Adams  counties,  there  is  no  distinct  evidence 
that  the  newer  formations  ever  spread.  Another  large  portion,  in- 
cluding Waushara,  Marquette,  northern  Green  Lake,  western  Colum- 
bia, northern  Sauk  and  southern  Juneau,  well  away  from  the  re- 
gions of  the  newer  rocks,  was  originally,  beyond  doubt,  overlaid 
by  at  least  the  Lower  Magnesian,  this  formation  occurring  on  two  out- 
lying bluffs  in  the  northwest  corner  of  Marquette  county,  25  miles 
distant  from  the  main  area  of  that  formation.  There  are  again  small- 
er areas,  as  the  strip  along  the  Wisconsin  below  the  great  bend,  and 
the  district  about  the  head  waters  of  the  Catfish,  in  Dane  county, 
which  occur  altogether  within  the  country  of  the  newer  formations, 
and  have,  beyond  doubt,  been  reached  by  erosion  along  the  existing 
valleys. 

On  the  north,  the  main  area  occupied  by  the  lower  sandstone  is 
limited  by  the  larger  one  in  which  the  crystalline  rocks  are  at  the 
surface.  The  boundary  between  the  Potsdam  and  Archaean  areas 
is  quite  difficult  to  trace.  As  stated  on  a  previous  page,  the  streams 
flowing  southward  from  the  Archaean  area  cut  through  the  sandstone 
beds  down  to  the  crystalline  rocks,  for  many  miles  after  entering  the 
sandstone  district,  whilst  on  the  divides  between  the  streams  the  sand- 
stone stretches  as  far  north  into  the  Archaean  regions.  The  difficul- 
ties in  tracing  the  boundary  line  in  any  greater  detail  than  thus 
stated  lie  in  the  peculiar  irregularity  of  the  upper  face  of  the 
older  rocks,  which  may  bring  them  to  the  surface  at  any  point;  in 
the  once  greater  spread  northward  of  the  sandstone,  as  a  result  of 
which  it  is  liable  to  be  found  in  little  patches,  filling  the  depressions 
of  the  older  rocks;  and  in  the  heavy  coating  of  drift  that  conceals  the 
rock  beneath  over  considerable  areas.  To  these  difficulties  may  be 
Wis.  SUR.  — 34 


530  GEOLOGY  OF  CENTRAL  WISCONSIN. 

added  the  fact  that  the  country  is  largely  unsettled,  and  covered  by 
heavy  forests  and  swamps.  The  former  spread  northward  of  the 
sandstone  beyond  its  present  limits  is  indicated  by  the  occurrence  on 
the  highest  part  of  the  dividing  ridges  of  outliers  of  that  formation, 
100  to  200  feet  in  height,  and  also  by  the  occurrence  in  the  northern 
drift  of  large  quantities  of  loose  sand. 

Notwithstanding  these  difficulties,  it  is  believed  that  the  boundary 
line,  as  indicated  on  Atlas  Plate  XY,  Area  F.,  is  not  far  from  correct. 
The  principal  facts  upon  which  it  is  based  may  be  here  briefly  stated. 
On  the  east  side  of  Area  F.,  sandstone  is  seen  in  a  small  quarry  on  a 
ridge  on  the  west  side  of  Plover  river,  on  whose  bank,  just  east,  and 
at  points  all  along  whose  course  to  the  mouth,  the  crystalline  rocks  are 
exposed.  From  the  quarry  mentioned  to  Stevens  Point,  sandstone 
appears  to  underlie  the  surface.  At  Stevens  Point,  it  appears  at  the 
top  of  the  bank  on  both  sides  of  the  Wisconsin  river,  whose  bed  is  on 
crystalline  rocks.  A  short  distance  north  of  Stevens  Point,  on  the 
road  to  Wausau,  and  also  on  the  road  following  the  west  bank  of  the 
river,  crystalline  rocks  are  to  be  seen,  and  no  sandstone  is  met  with 
further  north.  The  Wisconsin  Central  Railroad  cuts  through 
sandstone  at  Stevens  Point,  but  farther  to  the  west  arid  north 
it  is  altogether  on  crystalline  rocks,  as  shown  by  several  cuts  between 
Stevens  Point  and  Junction  City.  The  Wisconsin  Valley  Railroad, 
from  Knowlton,  Marathon  county,  to  Centralia,  Wood  county,  is  also 
altogether  on  the  crystalline  rocks,  which,  for  the  most  part,  lie  near 
the  surface,  with  very  little  drift  covering.  Along  the  east  side  of 
the  Wisconsin,  below  Stevens  Point,  sandstone  5  to  40  feet  in  thick- 
ness is  constantly  to  be  seen  in  the  east  bank  of  the  river,  the  crystal- 
line rocks  appearing  in  the  river  bottom  as  far  as  Point  Bass,  Sec.  15, 
T.  21,  R.  5  E.,  Wood  county.  At  this  point  the  crystalline  rocks 
disappear,  and  the  sands-tone  in  turn  forms  the  river  bed.  North- 
ward from  Point  Bass,  along  the  west  bank  of  the  river,  sandstone 
shows  again,  at  intervals,  as  far  as  Centralia.  The  Wisconsin  Valley 
Railroad,  north  from  Centralia,  as  already  said,  is  always  on  the  older 
rocks,  but  a  considerable  thickness  of  sandstone  occurs  in  a  ridge  on 
the  south  side  of  Mosquito  creek,  Sees.  29  and  30,  T.  23,  R.  6  E. 
Farther  north,  along  the  line  between  sections  7  and  8  of  the  same 
town,  small  thicknesses  of  sandstone  fill  depressions  between  the 
ridges.  On  the  north  side  of  the  Wisconsin,  between  Mosquito  and 
Mill  creeks,  sandstone  occurs  at  several  points,  but  does  not  stretch 
far  north,  for  crystalline  rocks  are  at  surface  over  the  northern  parts 
of  T.  23,  R.  6  and  7  E.  Mill  creek  is  altogether  on  the  crystalline 
rocks.  Along  the  line  of  the  Green  Bay  and  Minnesota  'Railroad, 


THE  LOWER  SILURIAN  ROCKS.  531 

westward  from  Grand  Rapids  as  far  as  Merrillon,  Sec.  15,  T.  23,  R.  4 
W.,  Jackson  county,  thin,  shaly  sandstone  is  frequently  exposed  in 
low  cuts,  but  having  evidently  a  small  thickness  only,  for,  at  the  cross- 
ing of  Black  river,  gneiss  is  exposed,  as  also  on  Yellow  river,  a  short 
distance  north  of  the  railroad  crossing.  Between  Grand  Rapids  and 
Dexterville,  the  sandstone  does  not  stretch  far  north  of  the  railroad 
line,  for  along  the  wagon  road  between  the  two  places  granite  is  seen 
at  the  surface. 

On  Yellow  river  the  crystalline  rocks  are  first  exposed  about  two 
miles  above  the  railroad  crossing,  beyond  which  point  they  are  con- 
stantly exposed  in  the  bed  of  the  river,  sandstone  appearing  at  points 
on  the  west  bank  as  far  north  as  the  northern  side  of  town  24.  Rocky 
Run,  in  towns  23  and  24,  is  on  crystalline  rocks.  In  the  towns  on 
the  divide  between  Yellow  and  Black  rivers,  sandstone  appears  to  be 
generally  the  surface  rock,  the  Archaean  only  occasionally  appearing 
through  it.  All  along  the  road  from  the  crossing  of  Yellow  river,  on 
the  south  line  of  T.  25,  R.  2  E.,  Wood  county,  to  Neillsville,  in  Sec. 
14,  T.  24,  R.  2  TV.,  Clark  county,  the  country  is  generally  high  and 
heavily  drift-covered,  wells  passing  through  5  to  100  feet  of  drift 
into  sandstone.  Sandstone  is  also  occasionally  seen  at  the  surface,  as 
in  the  road  on  the  S.  E.  qr.  of  Sec.  12,  T.  24,  R.  1  TV.,  and  in  an  out- 
lying bluff  at  the  center  of  the  S.  E.  qr.  of  Sec.  12,  T.  24,  R.  1  E. 
Sandstone  also  occurs  in  angular  fragments  on  the  ridges  along  the 
west  fork  of  Yellow  river  in  T.  25,  ranges  1  and  2  E.  Further  north, 
in  towns  25  and  26,  ranges  1  E.  and  1  TV.,  drift  covers  the  rocks 
heavily,  and  the  exact  extent  of  the  sandstone  has  not  been  ascer- 
tained, as  indicated  by  the  blank  space  left  on  the  map.  O'Neil's 
creek,  in  T.  24,  ranges  1  and  2  TV.,  cuts  down  to  the  older  rocks.  On 
Sec.  11,  T.  24,  R.  2  TV.,  sandstone  occurs  by  the  side  of  the  road,  and 
again  in  a  high  outlier  on  Sec.  3,  of  the  same  town,  on  the  west  side 
of  Black  river.  Westward  from  this  outlier  the  country  shows  sand- 
stone at  the  surface.  Similar  bluffs  occur  in  T.  25,  R.  2  W.,  the  crys- 
talline rocks  showing  along  the  river,  and  at  least  one  such  bluff  oc- 
curs in  T.  26,  R.  2  W.,  its  exact  location  not  being  known  to  the 
writer.  In  T.  26,  ranges  3  and  4  W.,  sandstone  is  reported  by  Dr. 
Randall1  as  extending  as  far  as  the  Eau  Claire  river,  beyond  which  it 
is  absent.  At  the  crossing  of  Black  river,  one  mile  west  from  Neills- 
ville,  S.  TV.  qr.  of  Sec.  15,  T.  24,  R.  2  W.,  granite  is  exposed  in  the 
river,  and  is  overlaid  by  sandstone  in  the  banks.  Similar  conditions 
hold  all  along  the  river,  as  far  as  the  falls  in  T.  21,  R.  4  W.,  the 

>  Owen's  Geological  Survey  of  Wisconsin,  Iowa  and  Minnesota. 


532  GEOLOGY  OF  CENTRAL  WISCONSIN. 

Archaean  rocks  becoming  more  and  more  restricted  to  the  stream  bed, 
until  they  finally  disappear. 
The  boundary  between  the  Potsdam  and  Lower  Magnesian  areas 

is  much  more  easily  traceable,  it  being  possible  in  the  driftless  dis- 
trict to  map  it  with  almost  any  degree  of  accuracy,  the  only  limit  be- 
ing the  amount  of  lime  spent  in  following  its  windings.  In  drift- 
covered  regions  this  degree  of  accuracy  is  not  attainable,  but  a  dis- 
tinct break  in  the  topography  generally  suffices  to  give  the  line  very 
closely.  It  has  already  been  said  that  in  the  Central  Wisconsin  dis- 
trict there  occur  well-marked  beds  of  passage  between  the  Lower 
Magnesian  and  the  Potsdam,  whose  surface  distribution  has  been 
separately  mapped.  These  layers,  however,  only  occasionally  have  a 
wide  surface  spread,  appearing  generally  on  the  steep  flanks  of  the 
higher  ground  occupied  by  the  Lower  Magnesian,  and  thus  forming 
on  the  map  a  narrow  strip  along  the  outer  edge  of  the  Lower  Magne- 
sian area.  The  limits  of  the  Lower  Magnesian,  and  of  the  beds  of 
passage,  are  so  close  together  that,  in  a  general  description  like  the 
present,  they  may  be  regarded  as  one.  On  the  east  we  find  this 
boundary  without  the  limits  of  the  Central  Wisconsin  district  until 
the  northern  line  of  Columbia  county  is  reached.  This  county  it 
crosses  in  an  irregular  line,  curving  from  northeast  to  southwest,  and 
marked  by  a  prominent  and  deeply  indented  escarpment.  North  and 
west  of  this  line  the  country  shows  everywhere  the  Potsdam  as  the 
surface  formation,  except  on  the  summits  of  the  numerous  outliers 
which  flank  the  escarpment.  At  the  southwest  corner  of  Columbia 
county,  the  Wisconsin  enters  upon  the  territory  of  the  Lower  Mag- 
nesian, through  which  it  cuts,  however,  deeply  into  the  underlying 
sandstone,  so  that  along  the  valley  bottom  we  have  a  broad  strip  of 
the  latter  formation  at  surface,  and  along  the  numerous  tributary 
streams  on  each  side,  strips  of  greater  or  less  width.  In  the  Four 
Lake  country,  about  the  city  of  Madison,  the  upper  layers  of  the 
Lower  sandstone  are  again  brought  to  the  surface  by  a  different  sys- 
tem of  erosion,  that  of  one  of  the  main  branch  streams  of  Rock  river. 
The  valley  surface  is  never,  however,  more  than  30  to  50  feet  below 
the  summit  of  the  sandstone  (the  Mendota  base),  and  south  of  Lake 
Monona  the  southerly  dip  carries  even  the  uppermost  beds  below  the 
valley  bottom.  In  Sauk  county,  north  of  the  Wisconsin,  the  boundary 
of  the  main  Potsdam  area  follows  the  west  side  of  the  town  of  Honey 
Creek,  then  bending  around  the  western  end  of  the  Baraboo  quartzite 
ranges,  in  the  towns  of  Westfield  and  Honey  Creek,  crosses  Eeedsburg, 
Ironton,  La  Yalle  and  Woodland,  in  a  northwesterly  direction  along 
the  west  side  of  the  valley  of  the  Baraboo  river  to  the  very  south- 


THE  LOWER  SILURIAN  ROCKS.  533 

western  corner  of  Juneau  county.  This  line  is,  however,  anything 
but  a  regular  one,  the  Lower  Magnesian  occurring  in  more  or  less 
detached  areas  crowning  the  summits  of  the  higher  grounds.  In 
Juneau  county  only  a  few  small  summits  in  the  southwest  corner 
reach  the  Lower  Magnesian  horizon,  the  rest  of  the  county  being 
well  down  in  the  Potsdam  series.  West  of  Juneau  county  the 
boundary  is  without  the  Central  Wisconsin  district. 

The  topographical  characters  of  the  regions  in  which  the  Pots- 
dam is  the  surface  rock  have  already  been  generally  given  in  the 
chapter  on  Surface  Features,  and  further  details  are  given  in  the 
latter  half  of  the  present  chapter.  It  may  be  said,  in  general,  that 
where  this  formation  is  at  surface  there  is  usually  a  loose,  sandy, 
sterile  soil,  a  sparse  growth  of  small  oak  timber,  mingling  with  and 
becoming  replaced  by  small  pine  towards  the  north,  and  a  general 
plain-like  character,  the  plain  dotted  with  lofty  and  rocky  outliers 
of  the  same  formation,  or  of  the  next  higher  one.  To  these  general 
statements  there  are  exceptions,  the  principal  of  which  .may  be  here 
given.  Excellent  soil  is  found  within  the  Potsdam  area  where  the 
drift  covering  is  heavy,  as  in  parts  of  Waushara  county,  or  where 
alluvial  depositions  exist  in  the  valley  bottoms,  as  in  places  along 
the  Wisconsin  valley,  or  yet  again  where  a  rough,  ridgy  charac- 
ter to  the  country  prevails,  as  in  southwestern  Juneau  county,  where 
good  land  occurs  on  the  top  of  the  ridges,  being  due  possibly  to  the 
tendency  of  the  loosened  sand  to  wash  downwards  towards  the  valleys. 
To  the  general  plain-like  character  of  the  Lower  sandstone  area,  south- 
western Juneau.  county  and  northwestern  Sank  make  an  exception, 
the  Baraboo  river  and  its  tributaries  having  worn  the  ridge  that  bounds 
the  central  sand  plain  into  an  adruptly  ridgy  country.  Another  ex- 
ception is  found  in  parts  of  Waushara  county,  where  morainic  drift 
occurs  in  great  abundance. 

The  general  lithological  characters  and  stratigraphical  ar- 
rangement of  the  Lower  sandstone  series  will  be  best  understood 
from  a  brief  summary  of  the  main  facts  obtained  in  the  different  dis- 
tricts in  which  the  formation  is  at  surface. 

At  Madison,  Dane  county,  the  Artesian  well  in  the  Capitol  park 
passes  through  126  feet  of  loose  materials,  apparently  all  belonging 
to  the  Drift,  704:  feet  of  sandstone,  for  the  most  part  purely  silic- 
ious,  light-colored,  and  fine-grained,  the  constituent  grains  being 
all  more  or  less  rolled,  and  cemented  by  a  varying,  but  always 
very  small,  amount  of  hydrous  iron  oxide  —  and  10  feet  of  a  red  shale, 
underneath  which  are  the  crystalline  rocks.  Similar  results  are  ob- 
tained from  the  well  at  the  Milwaukee  and  St.  Paul  depot  at  Madi- 


534  GEOLOGY  OF  CENTRAL  WISCONSIN. 

son,  the  summit  of  this  well  being  at  a  lower  level,  and  the  drift  TO 
feet  in  thickness.  In  the  former  well,  the  top  of  the  rock  is  63  feet, 
in  the  latter,  100  feet  below  the  base  of  the  Mendota  limestone,  as  ex- 
posed in  the  neighborhood.  On  the  banks  of  Lake  Mendota,  near 
Madison,  we  find  exposed,  beneath  this  limestone  and  above  the  lake 
level,  one  foot  of  greensand  and  31  feet  of  fine-grained,  light  green- 
ish, very  friable,  sandstone,  including  very  thin  dolomitic  seams,  and 
carrying  throughout  some  dolomitic  and  calcareous  matter,  the  con- 
tent of  purely  silicious  sand  being  84.45  per  cent.  Altogether,  then, 
we  find  in  the  Madison  region,  the  following  succession  of  layers 
between  the  Mendota  base  and  the  Archaean: 

Feet. 

1.  Greensand  layer 1 

2.  Calcareous  and  dolomitic,  friable,  fine-grained,  greenish,  sandstone  ...  31 

3.  Not  known 31 

4.  Light  colored  sandstone,  for  the  most  part  purely  silicious,  being  made 

of  rolled  quartz  grains;  but  no  specimens  obtained  from  the  upper- 
most layers 704 

5.  Red  shale 10 


Total 777 

Along  the  Wisconsin  river  bluffs  in  Columbia,  Sank  and  Dane 
counties,  the  Mendota  horizon  is  very  prominent,  the  sandstone 
showing  below  it  for  a  thickness  of  150  to  200  feet.  The  very  bold 
bluff  that  rises  from  the  north  bank  of  the  Wisconsin  river  at  the 
mouth  of  Honey  Creek,  in  the  town  of  Prairie  du  Sac,  Sauk  county, 
shows  the  following  section,  from  the  Mendota  base  downwards: 

Ft.    In. 

1.  Greensand  with  thin,  brown,  calcareous  layers;  the  greensand  layers  made 

up  of  fine  grains  of  glauconite  and  white  sand,  mingled  with  crystalline 

calcite 3     . . 

2.  No  exposure 7 

3.  Fine-grained  green  and  brown  sand,  calcareous 2      2 

4.  Loose  white  and  brown  sand,  some  layers  partly  calcareous 10     . . 

5.  Firm  and  heavy  layers  of  yellowish,  porous,  calcareous,  sandstone,  inter- 

stratified  with  layers  of  white  sand 6      3 

C.  Alternations  of  pure  white,  non-calcareous,  fine-grained  sand,  with  nodular- 
weathering,  yellow,  calcareous  layers,  and  layers  of  dark  greensand,  the 
whole  showing  fine  cross-lamination;  the  white  sand  layers  predominating,  45  . . 

7.  Fine-grained  light-colored  sandstone;  often  pure  white,  and  loose;  in  parts 

cross-laminated,  the  lines  of  cross -lamination  being  marked  by  rows  of 

glauconite  grains 9  6 

8.  Porous,  yellowish-brown,  slightly  calcareous  layers 4  11 

9.  No  exposure 11  6 

10.  Fine-grained,  friable,  greyish  sandstone,  only  slightly  calcareous,  carrying 

,a  few  yellow  calcareous  layers  as  above. 11      5 

11.  Finn  layers  of 'ferruginous  sandstone,  more  calcareous  than  the  last .- . .       5      6 


THE  LOWER  SILURIAN  ROCKS.  535 

Ft.    In. 

12.  Loose  brown  sand • 11 

13.  Unexposed 7     .. 

14.  Porous  and  crystalline-textured,  yellow  limestone,  with  much  coarse  and 

bright  green  glauconite 1 

15.  Unexposed 3      5 

16.  Like  No.  14,  interstratified  with  bright  green  seams 2      4 

17.  Heavy  brown  layer  of  slightly  calcareous  sandstone 3 

18.  Greensand  layer;  a  mixture  of  very  fine  white  sand  and  glauconite  grains, 

with  some  crystalline  calcite 10 

19.  Light  yellow,  friable  sandstone;  only  slightly  calcareous;  cross- laminated,      5      4 

20.  Greensand  layer,  like  18,  false  bedding  very  marked,  cross-laminae  very 

plain 13 

21.  Porous,  yeUow,  slightly  calcareous  sandstone 6 

22.  Fine-grained,  cross-laminated,  slightly  calcareous  sandstone,  with  much 

greensand 1     11 

23.  Greensand,  like  No.  20 10 

24.  Fine-grained,  friable,  white  sandstone,  slightly  calcareous 1 

25.  Unexposed. 12      7 

26.  Fine-grained,  white  sandstone,  entirely  non-calcareous;  made  up  altogether 

of  fine  rounded  grains  of  limpid  quartz 22 

Total..  .  189      3 


The  horizon  of  the  base  of  this  section  is  146  feet  below  the  top  of 
the  rock  in  the  capitol  well  at  Madison,  thus  covering  the  gap  in  the 
Madison  section.  Combining  the  two  sections,  we  obtain  for  the 
whole  series  the  following  general  succession : 

Feet. 

1.  Alternations  of  layers  of  purely  silicious  white  sand,  ferruginous  brown  sand, 

yellowish  calcareo- arenaceous  layers,  and  layers  of  greensand;  the  calcareous 
bands  increasing  in  amount  of  lime  and  in  number  towards  the  top,  as  is  also 
the  case  with  the  greensand  layers 165 

2.  Entirely  non-calcareous,  white  and  yellow,  sandstone;  friable  to  indurated;  fine 

to  coarse-grained 602 

3.  Red  shale 10 


Total 777 


The  calcareous  layers  have  never  been  observed  extending  more 
than  150  feet  below  the  Mendota  base.  The  "greensand"  layers 
mentioned  are  mixtures  of  green  grains  of  a  mineral  probably  closely 
allied  to  the  glauconite  of  the  Cretaceous  formation,  rounded  grains 
of  quartz,  and  usually  more  or  less  of  angular  pieces  of  calcite.  These 
layers  are  very  characteristic  of  the  lower  sandstone,  occurring,  ac- 
cording to  Dr.  Owen,  at  many  different  horizons  throughout  the  series 
as  developed  along  the  Mississippi.  In  Central  Wisconsin,  however, 
none  have  been  recognized  more  than  160  feet  below  the  Mendota 
base.  No  chemical  investigation  of  Central  "Wisconsin  greensand  has 
ever  been  made,  but  Dr.  T.  S.  Hunt  has  given  an  analysis  of  a  green- 


536  GEOLOGY  OF  CENTRAL  WISCONSIN. 

sand  from  the  Lower  Magnesian  limestone  of  Minnesota,  at  Red  Bird, 
on  the  Mississippi,  which  is  beyond  doubt  the  same  material.  This 
analysis  (I),  as  also  another,  by  the  same  gentleman,  of  the  Cretace- 
ous greensand  of  New  Jersey  (II),  is  given  below:1 

I. 

Silica 46 . 58 

Alumina 1 1 . 45 

Iron  protoxide 20.61 

Magnesia 1 .27 

Lime 2.49 

Soda 0.98 

Potash 6.96 

Water...  9.66 


100.00         100.00 


The  green  grains  of  both  Cretaceous  and  Silurian  greensands,  as 
also  of  similar  deposits  in  existing  seas,  are  often  found  as  casts  of 
the  shells  of  rhizopods.  So  far  as  the  writer's  knowledge  goes  no 
such  observation  has  ever  been  made  with  regard  to  the  Wisconsin 
greensand.  The  greensand  layers  are  by  no  means  restricted  to  the 
Potsdam  series;  they  occur  in  both  the  Lower  Magnesian  and  St. 
Peters.  Greensand  grains  occur  also  apart  from  the  regular  green 
layers.  The  thin,  yellow  and  brown,  rough-textured,  calcareous 
bands,  that  characterize  the  layers  immediately  beneath  the  Mendota, 
are  often  dotted  with  coarse  grains  of  glauconite,  which  are  not  in  suf- 
ficient quantity  to  impart  their  color  to  the  rock. 

The  generalized  section  given  above  for  the  Potsdam  series,  below 
the  Mendota  base,  holds  true  for  a  large  part  of  the  Central  Wiscon- 
sin district,  and  would  be  satisfactory  for  all  of  it,  but  for  the  facts 
next  to  be  stated.  Proceeding  northward  from  the  valley  of  the  Wis- 
consin, we  encounter,  traversing  Sauk  and  eastern  Columbia  counties 
for  25  miles  from  east  to  west,  the  Archaean  quartzite  ranges  described 
in  the  last  chapter.  The  Mendota  horizon  continues  well  marked  di- 
rectly up  to  the  ranges,  whilst  in  the  country  west  and  east,  it  extends 
much  further  to  the  northward.  Everywhere  about  the  quartzite, 
however,  we  find,  lying  uncoriformably  upon  it,  layers  of  sandstone 
and  bowlder-conglomerate,  which,  as  regards  altitude,  appear  to  oc- 
cupy the  entire  distance  between  a  horizon  considerably  below  the 
Mendota,  and  one  nearly  as  high  as,  if  not  higher  than,  the  summit  of  the 
Lower  Magnesian.  These  layers  of  sandstone  and  conglomerate  can- 
not, in  all,  be  less  than  400  feet  in  thickness,  being  nearly  always 
without  calcareous  admixture.  Single  cliffs  occur  showing  225  feet 

1  Geology  of  Canada,  p.  488. 


THE  LOWER  SILURIAN  ROCKS.  537 

of  friable,  entirely  non-calcareous,  sandstone,  the  summits  far  above 
any  apparently  possible  position  of  the  Lower  Magnesian,  whilst  be- 
low their  bases  numerous  other  sandstone  exposures  occur,  carrying 
the  sandrock  down  further.  Nor  are  these  occurrences  of  thick  and 
high-level  sandstone  at  any  considerable  distances  from  points  where 
the  regular  succession  of  Lower  Magnesian,  Madison  and  Mendota  is 
to  be  observed.  In  places  in  the  town  of  Westfield,  on  the  western  end 
of  the  quartzite  ranges,  it  is  possible  to  pass  within  a  quarter  of  a 
mile  from  Mendota  limestone,  occupying  its  normal  position,  to  sand- 
stone ledges  which  rise  from  the  same  level  for  over  250  feet. 

As  already  described,  the  quartzite  ranges  almost  completely  en- 
circle the  intervening  valley,  whose  altitude  is  somewhat  greater  than 
that  of  the  surrounding  outside  country.  Within  the  valley,  non- 
calcareous,  occasionally  much-indurated,  sandstone,  with  local  con- 
glomerate beds,  is  to  be  seen  at  almost  all  levels  to  the  summits  of 
the  quartzite  ranges,  but  at  two  points  limestone  is  known  to  occur. 
These  localities  are  described  fully  in  a  subsequent  page.  It  is  now 
merely  necessary  to  say  that  at  one  of  tb.3  places,  on  the  south  flank 
of  the  north  quartzite  range,  near  the  Lower  Narrows  of  the  Baraboo, 
are  to  be  seen  20  feet  of  limestone,  containing  a  number  of  fossils, 
mostly  of  new  species,  which  Mr.  R.  P.  Whittield  regards  as  unques- 
tionably not  lower  than  the  Lower  Magnesian.  Below  on  the  side- 
hill  are  numerous  but  not  continuous  exposures  of  sandstone,  those 
nearest  the  limestone  evidently  forming  the  next  lower  layer,  and  re- 
sembling closely  the  Madison  beds.  Across  the  valley,  one-half  mile 
southeastward,  is  a  vertical  cliff  of  red-and-white-banded,  fine-grained, 
friable  sandstone,  rising  from  75  to  165  feet  above  the  summit  of  the 
limestone,  whose  altitude  is  what  would  be  expected  for  the  Lower 
Magnesian,  from  the  occurrences  of  that  formation  a  few  miles  to  the 
southward.  One  mile  further  west  sandstone  and  bowlder-conglom- 
erate, flanking  the  quartzite,  rise  similarly  above  the  limestone. 

At  the  other  point,  not  far  from  the  village  of  Baraboo,  and  on  the 
north  slope  of  the  south  quartzite  range,  exactly  similar  limestone  is 
found,  without  fossils,  covering  a  small  summit,  and  underlaid  by  ferru- 
ginons,  fine-grained  sandstone,  carrying  Scolithus  and  Dicellocephalus 
Minnesotensis.  At  a  still  lower  level,  near  by,  a  fine-grained,  yel- 
lowish, aluminous  limestone  occurs,  the  three  different  layers  having 
just  the  characters  and  relative  positions  for  the  Lower  Magnesian,  Mad- 
ison and  Mendota  beds.  Below  the  lowest  limestone  layer,  and  within 
a  few  rods  of  it,  are,  however,  ledges  of  much  indurated,  non-cal- 
careous rock,  entirely  unlike  the  friable  dolomitic  sandstone  normally 
occurring  beneath  the  Mendota.  Three  miles  south  of  east  from  here, 


538  GEOLOGY  OF  CENTRAL  WISCONSIN. 

about  Devil's  Lake,  the  high  level  sandstones,  with  bowlder-conglom- 
erate beds,  are  again  found,  with  a  total  thickness  exposed  of  over  300 
feet,  the  base  being  nearly  on  a  level  with  the  lowest  of  the  limestones 
at  the  locality  just  described.  In  one  place,  a  short  distance  north- 
east of  Devil's  Lake,  large  loose  masses  of  this  sandstone  occur  at  an 
altitude  between  100  and  150  feet  above  the  last  named  limestone, 
carrying  fossils,  among  which  are  Dicellocephalus  Minnesotensis  and 
others  supposed  to  indicate  the  upper  layers  of  the  Potsdam  series. 

For  these  anomalous  occurrences,  which  will  be  more  fully  under- 
stood from  a  study  of  the  sections  of  Plates  XIX  and  XX,  and  Figs. 
48  and  49  of  this  volume,  and  of  the  detailed  descriptions  in  the  fol- 
lowing pages,  it  is  not  easy  to  find  a  satisfactory  explanation.  It  ap- 
pears altogether  inadmissible  to  attribute  the  great  elevation  of  the 
high-level  sandstone  to  a  sudden  affection  of  the  nearly  horizontal 
strata  by  a  violent  northern  rise  as  they  near  the  quartzite  ranges. 
This  supposition  is  forbidden  by  the  utter  lack  of  any  indication  01 
such  a  rise  in  the  large  exposures  that  occur;  by  the  normal  success- 
ion of  beds  that  holds  true  in  all  the  region  east,  west  and  north  of 
the  quartzite  ranges;  and  by  the  great  amount  of  rise  that  would  be 
necessary.  In  "Westfield  it  would  have  to  be  300  to  400  feet  to  the 
mile.  Moreover,  within  the  space  enclosed  by  the  quartzite  ranges, 
as  described,  occur  the  Lower  Magnesian,  Madison  and  Mendota,  in 
their  normal  succession,  and  with  their  normal  lower  level,  whilst  in 
one  case  the  limestone  and  perfectly  horizontal  high-level  sandstone 
are  so  near  by  that  no  amount  of  dip  could  possibly  account  for  the 
occurrence.  It  may  be  regarded  as  beyond  question  that  entirely 
non- calcareous  sandstone  writh  bowlder-conglomerate  and  Potsdam 
fossils  does,  not  only  apparently,  but  actually,  occupy  the  whole  space 
between  the  horizon  of  the  base  of  the  Mendota,  and  that  of  the  sum- 
mit of  the  Lower  Magnesian. 

It  might  be  supposed  that  the  wear  of  the  quartzite  ranges  contin- 
ued to  produce  sandstone  and  conglomerate  beds  during  the  growth 
of  the  limestone  in  the  deeper  water  near  by,  but  the  suddenness  of 
the  transitions,  the  occurrence  of  Potsdam  fossils  in  the  sandstone, 
and  the  existence  of  the  limestone  layers  close  to  and  within  the 
quartzite  ranges,  appear  great  difficulties  in  the  way  of  such  an  ex- 
planation. That  the  high-level  sandstones  represent  really  an  older 
series,  upon  whose  eroded  upper  surface  rest  the  calcareous  sandstone 
of  the  Potsdam,  the  Mendota,  the  Madison,  and  the  Lower  Magnesian, 
as  indicated  in  the  ideal  sketch  of  Fig.  34,  appears  a  more  satisfactory 
explanation,  but  one  which  meets  a  considerable  difficulty  in  the  oc- 
currence of  upper  Potsdam  fossils  in  the  high-level  beds,  and  one 


THE  LOWER  SILURIAN  ROCKS. 


539 


which  I  am  somewhat  loath  to  advance,  as  too  bold  a  generalization 
from  the  facts  in  hand.  It  is  not  impossible  that  the  true  explana- 
tion may  lie  in  the  supposition  that  during  the  deposition  of  the  Pots- 
dam series  the  quartzite'  ranges,  being  high  islands  and  reefs  in  the 
ancient  seas,  received  synchronous  littoral  depositions  at  high  and  ab- 
normal altitudes,  the  sand  and  bowlders  for  these  depositions  coining 
from  the  wear  of  the  quartzite  itself. 

Leaving  now  the  Baraboo  region,  and  proceeding  northward  along 
the  eastern  side  of  the  district,  we  find,  everywhere  in  the  neighbor- 
hood of  the  escarpment  that  forms  the  western  edge  of  the  main  area 
of  the  Lower  Magnesian,  the  same  succession  of  layers  as  seen  along 
the  Wisconsin  in  Columbia  and  Sauk  counties,  i.  e.,  Madison  and 
Mendota  beds,  underlaid  by  100  to  150  feet  of  calcareo-arenaceous 
layers,  and  these  again  by  brown  and  white  non -calcareous  sandstone. 
This  succession  holds  true  at  least  as  far  as  Waupaca  county,  and 
probably  further  than  this.  West  of  the  escarpment,  in  Wausharn, 
Marquette  and  Columbia  counties,  the  country  surface  is  generally 

FIG.  34. 


IDEAL  STRUCTURAL  SKETCH,  SHOWING  POSSIBLE  RELATIONS  OF  THE  HORIZONTAL  FORMA TIOJIH  IM 
THE  VICINITY  OP  THE  BARABOO  QUARTZITE  RANGES. 

well  down  in  the  Potsdam,  and  much  drift-covered.  In  central  Wau- 
shara  county,  however,  are  some  high  hills  reaching  into  the  limy 
beds  just  beneath  the  Mendota,  and  showing  the  normal  succession 
of  layers;  whilst  in  the  very  northeast  corner  of  Marquette  county,  25 
miles  from  the  boundary  of  the  main  Lower  Magnesian  area,  are  two 
isolated  bluffs,  capped  by  that  formation,  which  show  also  the  usual 
layers.  It  is  thus  evident  that  for  all  this  region  there  are  no  de- 
partures from  the  Madison  section.  At  several  points  in  Marquetto 
and  Waushara  counties  quarries  are  opened  in  beds  that  lie  about  200 
feet  below  the  Mendota,  and  yield  a  much  indurated,  white  sandrock, 
which  is  occasionally  quite  coarse,  and  is  made  up  of  nearly  glassy 
quartz  pebbles. 

Proceeding  now  westward  into  Adams  and  Juneau   counties,  we 
find  again  some  apparently  abnormal  occurrences.     One  mile  west 


540  GEOLOGY  OP  CENTRAL  WISCONSIN. 

from  the  lime-capped  bluffs  at  the  northwestern  corner  of  Marquette 
county,  are  other  bluffs,  showing  large  exposures  of  the  limy  layers 
that  come  immediately  beneath  the  Mendota.  One  and  a  half  miles 
northwest  from  here,  on  Sec.  3,  T.  17,  R.  7  E.,  across  an  intervening 
level  stretch  of  sand,  is  one  of  the  towers  of  sandstone  that  char- 
acterize the  central  plain  —  known  as  Pilot  Knob.  This  peak  rises 
25  feet  above  the  top  of  the  calcareous  layers  seen  just  across  the 
valley,  and  65  feet  above  their  base,  and  yet  from  its  summit  down 
for  150  feet,  we  find  only  altogether  non-calcareous  sandstone,  much 
of  which  is  highly  ferruginous,  and  all  of  which  is  quite  unlike  anj 
of  the  layers  that  are  usually  found  within  200  feet  of  the  base  of  the 
Mendota.  Moreover,  two  fossil  horizons,  yielding  Ptychaspis  Mitiis- 
caensis,  and  other  forms,  supposed  to  be  characteristic  of  the  middle 
portion  of  the  lower  sandstone,  occur  in  this  exposure.  We  have, 
then,  here,  to  some  extent,  a  repetition  of  the  anomalous  occurrences 
of  the  Baraboo  region — noncalcareous,  red,  ferruginous  sandstone,  with 
fossils  indicating  a  horizon  full  300  feet  below  the  Mendota,  rising 
through  the  horizon  of  the  upper  calcareous  beds,  into  that  of  the 
Mendota.  Some  nine  miles  west  of  Pilot  Knob,  near  Friendship, 
Adams  county,  occur  other  similar  sandstone  towers,  all  showing  en- 
tirely non-calcareous,  friable  rock.  On  the  summit  of  one  of  them, 
the  Roche  a  Cris,  is  to  be  recognized  the  uppermost  of  the  fossil 
horizons  of  Pilot  Knob,  the  lower  one  of  which,  marked  by  a 
peculiar  lithological  character,  is  still  more  unmistakably  to  be  re- 
cognized on  another  bluff,  some  five  miles  south  of  Friendship.  Both 
of  these  horizons  indicate  a  slight  rise  of  the  layers  eastward  towards 
Pilot  Knob.  Still  another  one  of  these  outliers,  the  Friendship 
Mound,  rises  85  feet  higher  than  the  Roche  a  Cris  near  by,  carrying 
the  light-colored,  friable,  non-calcareous  sandstone  all  the  way.  The 
horizon  of  the  summit  of  this  bluff  is,  then,  85  feet  above  that  of  the 
summit  of  Pilot  Knob,  or,  if  the  latter  rises  into  the  horizon  of  the 
Mendota,  as  high  as  the  position  that  would  be  expected  for  the 
Lowrer  Magnesian,  from  its  occurrences  in  northeast  Marquette 
county. 

At  the  southern  end  of  Adams  county,  the  Wisconsin  passes  the 
gorge  known  as  the  Dalles.  At  the  northern  end  of  the  gorge  is 
another  of  the  large  sandstone  outliers  like  those  just  mentioned  — 
the  Elephant's  Back.  This  bluff,  with  the  walls  o£  the  gorge  below, 
gives  a  nearly  continuous  section  of  310  feet.  At  Kilbourn  City,  two 
miles  below,  an  Artesian  boring  penetrates  into  the  underlying  Arch- 
aean. Combining  the  results  of  the  section  and  boring,  we  have  the 
following  general  succession : 


THE  LOWER  SILURIAN  ROCKS.  541 

Fine-grained  sand  layers;  of  varying1  colors,  in  upper  portions;  with  gaps  of  10  to 
70  feet;  including  at  base  some  quite  coarse-grained  sand  layers;  all  formed  of 

rolled  quartz,  and  aD  entirely  non-calcareous 310 

The  same  continued  in  the  Artesian  well 385 

Red  shale 15 

Total .~T10 


At  the  summit  of  the  Elephant's  Back,  fragments  of  trilobites 
occur  in  the  loose  sand  rock,  and  the  horizon  may  be  the  same  as  that 
on  the  top  of  Roche  a  Cris.  The  occurrence  here  of  the  same  red 
shale  as  observed  in  the  Madison  wells  is  worthy  of  notice.  The 
same  layer  has  been  reached  by  Artesian  borings  in  other  parts  of  the 
state. 

Returning  now  to  the  Baraboo  ranges  and  passing  northward  from 
their  western  ends  along  the  west  side  of  the  district,  we  find  in  the 
town  of  Reedsburg,  Sauk  county,  the  Lower  Magnesian,  Madison  and 
Mendota,  with  their  usual  characters.  In  the  same  town,  at  points 
some  miles  apart,  exposures  of  a  bed  of  red  shale  are  to  be  seen  whoso 
horizon  is  140  feet  below  the  Mendota  base.  Further  north,  in  north- 
western Juneau,  a  high,  ridgy  country  is  met  with,  carrying  sand- 
stone at  high  levels,  in  what  would  be  expected  to  be  the  Lower 
Magnesian  horizon.  This,  however,  appears  to  be  due  to  a  thicken- 
ing of  the  Madison  beds,  since  the  Lower  Magnesian  is  found  capping 
a  few  very  high  points,  and  the  Mendota  beds  below  continue  recog- 
nizable. In  southwestern  Juneau  county,  on  the  inner  side  of  the 
high  ground  bordering  the  central  plain,  are  numbers  of  isolated 
sandstone  outliers.  Some  of  these  show  a  bed  of  red  shale  and  soft 
greensand,  which  appears  to  be  the  same  as  that  seen  in  the  town  of 
Reedsburg.  This  greensand  layer,  about  130-140  feet  below  the 
Mendota,  is  the  lowest  seen  anywhere  in  the  Potsdam  series  of  Cen- 
tral Wisconsin. 

Still  further  north,  the  country  is  generally  eroded  well  down  into 
the  middle  of  the  Lower  sandstone,  so  that  the  Archaean  rocks  are  not 
very  far  beneath  the  surface,  which  they  come  nearer  and  nearer  to, 
towards  the  north.  Over  much  of  Portage,  Wood,  Jackson  and  Clark 
counties,  the  thickness  of  the  sandstone  cannot  be  more  than  25  to 
60  feet.  In  places  in  this  region,  the  sandstone  lying  within  20  to  40 
feet  of  the  crystalline  rocks  is  a  much  indurated,  coarse,  white  rock, 
which  yields  a  valuable  quarry  stone,  and  appears  to  occupy  the  same 
horizon  as  a  similar  rock  in  Waushara  and  Marquette  counties.  It  is 
probably  to  be  referred  nearly  to  the  middle  part  of  the  Lower  sand- 
stone. The  sandstone  immediately  in  contact  with  the  crystalline 


54:2  GEOLOGY  OF  CENTRAL  WISCONSIN. 

rocks  is  usually  a  quite  friable,  fine  to  coarse-grained,  brownish  rock, 
containing  pebbles  from  the  rock  below. 

It  is  not  at  all  impossible,  as  already  indicated,  that  the  anomalous 
occurrences  about  the  Baraboo  quartzite  ranges,  and  in  Adams  county, 
may  mean  that  the  Lower  sandstone  really  consists  of  two  series,  the 
one,  including  the  ordinary  calcareous  sandstone  that  comes  beneath 
the  Mendota,  and  an  unknown  thickness  below,  resting  upon  the 
eroded  surface  of  the  other.  Dr.  Owen  gives  sections  from  the  St. 
Croix  region,  showing  the  Lower  Magnesian  occupying  positions 
lower  than  the  Potsdam  in  the  immediate  vicinity,  which  may  indi- 
cate the  same  thing.  These  occurrences  on  the  St.  Croix  are  also 
described  by  Dr.  Percival  in  some  detail,  he  considering  them  best 
explained  by  the  existence  of  several  alternations  of  limestone  and 
sandstone.  Still  more  strongly  confirming  the  idea,  are  the  occur- 
rences in  the  vicinity  of  the  Archaean  patches  at  Berlin,  in  Green 
Lake  county,  and  Portland,  in  Dodge  county,  as  described  to  me  by 
Professor  Chamberlin.  In  the  former  case,  a  mound  of  quartz- 
porphyry  projects  into  the  horizon  of  the  Lower  Magnesian,  but  is 
flanked  by  sandstone  containing  the  fossils  regarded  by  Hall  as  be- 
longing to  the  middle  Potsdam.  In  the  latter  case,  several  distinct 
mounds  of  Archaean  quartzite  lie  in  the  horizon  of  the  St.  Peters 
sandstone,  which  shows  on  the  margin  of  the^  low  ground  in  which 
the  mounds  occur.  Flanking  the  quartzite,  however,  are  layers  of  a 
bowlder-conglomerate  carrying  /Scolithus,  which  is  usually  regarded 
as  restricted  to  the  lower  sandstone.  It  is  quite  evident  that  even  if 
the  lower  sandstone  really  does  include  two  formations  so  distinct  in 
age  as  these  facts  seem  to  suggest,  such  a  division  of  the  series  would 
be  quite  difficult  to  demonstrate,  on  account  of  the  great  lithological 
similarity  between  the  two  divisions,  whilst,  if  proved,  the  separation 
of  the  two  in  mapping  would  be  even  more  difficult. 

The  beds  of  passage  between  the  Potsdam  and  Lower  Magnesian 
series  include,  as  already  said,  twro  well  marked  beds,  60  to  90  feet  in 
combined  thickness  —  the  Mendota  limestone  and  the  Madison  sand- 
stone—  which,  from  their  prominence  in  Central  Wisconsin,  are 
worthy  of  separate  mention.  For  the  most  part  these  layers  come  to 
the  surface  only  on  the  flanks  of  the  higher  levels  occupied  by  the 
Lower  Magnesian,  so  that  they  present  on  the  map  only  narrow  bands 
bordering  the  areas  of  the  last  named  formation.  In  that  part  of  the 
Catfish  valley,  however,  which  lies  between  the  southern  shores  of 
Lakes  Monona  and  Kegonsa,  they  are  at  the  surface  over  a  wide  area, 
whilst  in  some  parts  of  Columbia  county  the  belt  occupied  by  them 
sometimes  reaches  two  or  three  miles  in  width.  Both  beds  are  to  be 


THE  LOWER  SILURIAN  ROCKS.  543 

distinctly  recognized  throughout  the  Central  Wisconsin  district, 
wherever  the  base  of  the  Lower  Magnesian  can  be  inspected.  The 
northernmost  point  at  which  1  have  recognized  them  is  at  the  north- 
west corner  of  Marquette  county,  the  southernmost  on  the  south 
shore  of  Lake  Kegonsa  in  Dane  county;  the  two  points  being  about 
70  miles  apart.  The  most  distant  points  east  and  west  at  which  they 
have  been  seen  in  Central  Wisconsin  are  about  as  far  from  one 
another.  To  the  northeast,  however,  Prof.  Chamberlin  thinks  he  has 
recognized  the  Mendota  as  far  as  the  Michigan  line,  whilst  Mr.  Strong 
carries  the  same  layer  westward  to  the  Mississippi. 

The  Mendota  and  Madison  beds  often  have  a  marked  effect  upon 
the  topography,  producing,  by  their  different  hardnesses,  benches  in 
the  sides  of  bluffs.  Where  the  Mendota  is  at  surface  over  any  con- 
siderable area,  it  produces  generally  an  excellent  clayey  soil ;  whilst 
the  Madison  soils,  as  in  a  large  part  of  the  town  of  Otsego,  Columbia 
county,  are  as  loose  and  sandy  as  those  of  the  Potsdam  proper.  About 
Madison,  where  the  two  layers  were  first  distinctly  recognized,  the 
Mendota  has  a  thickness  of  30  to  35  feet,  of  which  the  lower  20  feet 
are  of  a  heavily-bedded,  dark -yellow  and  brown,  jointed,  conchoidal- 
fracturing  rock,  which  is  stained  in  seams  and  patches  by  the  red  oxide 
of  iron,  and  leaves  on  solution  3  to  10  per  cent,  of  an  aluminous  and 
non-arenaceous  residue.  This  rock  quite  closely  resembles  the  lower 
portions  of  the  Lower  Magnesian  proper,  having  sometimes  the  con- 
cretionary structure  characterizing  that  formation.  The  upper  part 
of  the  Mendota  about  Madison  resembles  the  lower,  except  in  being 
in  thin,  rough-surfaced,  layers,  and  in  carrying  a  somewhat  larger 
percentage  of  silicious  matter.  To  show  the  close  similarity  in  com- 
position which  this  phase  of  the  Mendota  bears  to  the  Lower  Magne- 
sian, the  following  analyses  are  given,  I  being  the  Mendota,  from  the 
quarry  near  Greenbush,  Madison,  and  II,  Lower  Magnesian  from 
Williams'  quarry,  on  the  south  line  of  the  town  of  Madison: 

I.  IT. 

Silica 4.18  1.09 

Alumina 2.17  .44 

Iron  sesquioxide 1 .45  .43 

Iron  protoxide -63 

Lime  cartxmate 55.68  66.82 

Magnesia  carbonate 36 . 52  30.40 

Water 58  .35 


100.58  100.26 


It  will  be  noticed  that  in  both  the  proportion  of  lime  to  magnesia 
carbonate  is  greater  than  in  true  dolomite  (1.19: 1).     Both  yield,  also, 


GEOLOGY  OF  CENTRAL  WISCONSIN. 

on  solution,  an  argillaceous  residue,  differing  in  this  regard  from  ihe 
limy  layers  of  the  Potsdam  proper,  which  always  yield  a  residue  of 
white  quartz-sand,  with  or  without  glauconite  grains.  The  close 
earthy  texture  of  the  Mendota  also  contrasts  greatly  with  the  porous 
and  highly  crystalline  character  of  the  lower  calcareous  seams. 

The  Madison  beds,  in  the  country  about  Madison,  are  about  35  feet 
thick,  and  consist  usually  of  pure  white,  frequently  loose,  sand,  over- 
laid by  brown  and  yellow,  firmer  rock.  The  upper  layers  show  gen- 
erally a  slight  calcareous  admixture,  which  locally  increases  to  10  or 
15  per  cent., -the  rock  then  becoming  a  good  building  material,  and 
not  being  very  sharply  defined  from  the  limestone  above.  The  calca- 
reous layers  show  well  in  the  quarry  just  west  of  the  city  of  Madison, 
where  they  are  as  much  as  15  feet  in  thickness,  and  also  in  the  large 
quarry  near  the  village  of  Middleton.  The  section  at  the  latter  place, 
given  in  detail  on  a  subsequent  page,  is  of  interest  as  showing  the 
gradation  of  the  Potsdam  series  into  the  Lower  Magnesian,  there  be- 
ing a  number  of  thin  alternating  sandstone  and  limestone  layers, 
whilst  the  upper  Madison  beds  contain  as  much  as  50  per  cent,  of 
lime  and  magnesia  carbonates.  West  of  Lake  Kegonsa,  in  the  town 
of  Dunn,  the  Madison  sandstone  is  as  much  as  50  feet  in  thickness, 
closely  resembling  the  St.  Peters,  and  grading  downwards  into  the 
Mendota. 

About  the  village  of  Lodi,  in  Columbia  county,  both  Madison  and 
Mendota  are  frequently  exposed,  with  characters  like  those  just  de- 
scribed. Further  northeast,  along  the  western  edge  of  the  Lower 
Magnesian,  they  undergo  some  change.  At  Rio  the  lower  portions 
of  the  Madison  are  composed  of  a  firm,  white,  purely  silicious  mate- 
rial, which  is  made  up  of  sharply  angular  quartz,  whilst  above,  the 
ordinary  brown,  fine-grained  rock  comes  in.  Near  Cambria,  still 
farther  north,  the  same  thing  is  to  be  seen,  the  Mendota  layers  be- 
coming at  the  same  time  largely  replaced  by  reddish  clay-shale,  but 
still  retaining  in  parts  the  typical  yellow  appearance.  Near  Mar- 
quette,  in  Green  Lake  county,  the  Madison  has  its  usual  brownish, 
friable  character,  whilst  the  Mendota  is  largely  composed  of  a  light 
yellow,  regularly  bedded,  aluminous  limestone,  and  is  not  well  defined 
from  the  sandstone  below. 

Along  the  valley  of  the  Wisconsin,  in  Sauk  and  Dane  counties,  both 
of  the  layers  are  well  marked,  the  Mendota  having  most  commonly 
the  character  last  described.  Its  regular  bedding  makes  it  valuable 
as  a  building  stone,  and  it  is  hence  frequently  quarried.  Near  Spring 
Green  it  reaches  a  thickness  of  as  much  as  45  feet  in  all,  its  upper 
layers  being  shaly  and  fossiliferous.  The  Madison  sandstone  in  this 


THE  LOWER  SILURIAN  ROCKS.  545 

section  has  also  an  increased  thickness,  reaching  45  feet,  hut  other- 
wise it  shows  the  characters  before  noted.  Northward,  along  the  west 
side  of  Sank  county,  both  layers  continue  well  marked  as  far  as  the 
Bamboo  river.  Still  farther  north  the  Madison,  beds  thicken  to  60 
feet,  are  made  up  of  fine-grained,  red  and  white,  saccharoidal  sand- 
stone, closely  resembling  the  St.  Peters,  and  have  at  top  one  or  two 
feet  of  cherty  quartzite-like  material. 

To  the  list  of  fossils  of  the  lower  sandet3ne  series  given  by  Hall, 
but  little  has  been  added  by  the  present  survey,  as  far  as  Central  Wis- 
consin is  concerned.  It  has  already  been  said  that  his  general  group- 
ing, of  upper,  middle,  and  lower  species,  appears  to  hold  true  as  re- 
gards the  order,  but  that  his  lower  species  must  really  be  assigned  to 
the  middle  of  the  series,  since  its  thickness  is  about  twice  as  great  as 
Mr.  Hall  supposed.  Fossils  are  not  plenty  in  the  Central  Wisconsin 
Potsdam.  In  the  ordinary  non-calcareous  rock  they  occur  as  mere 
ferruginous  coatings  on  the  loose  sand,  trilobite  fragments  being  the 
most  common.  In  the  upper  shaly  layers  of  the  Mendota  beds,  very 
large  impressions  of  Dicellocephalus  Minnesotensis  are  quite  abund- 
ant. The  pygidium  is  most  frequently  found,  some  specimens  meas- 
uring as  much  as-  six  inches  across.  The  same  fossil,  however,  is 
found  in  the  loose  friable  sandstones  that  lie  upon  the  quartzites  of 
the  Baraboo  ranges,  and  not  improbably  has  a  considerable  vertical 
range,  since  it  is  quoted  by  Hall  from  the  Lower  Magnesian  of  Min- 
nesota. One  new  fossil  of  some  interest  has  been  added  to  Hall's 
list.  This  is  a  very  large  new  species  of  the  genus  Palc&acmea,  which 
was  originally  established  by  Hall  and  Whit-field,  in  1867,  to  cover  a 
"conical,  patelliform,  univalve  shell,"  which  occurs  in  the  Potsdam 
sandstone  of  New  York.  The  Wisconsin  species  is  twice  as  large  as 
that  from  New  York,  and  is  found  in  a  very  hard  quartzite,  which 
occurs  interstratified  with  loose,  friable  sandstone  on  the  Trempealeau 
river,  in  Jackson  county,  in  the  middle  portion  of  the  Potsdam  series. 

The  economic  contents  of  the  Lower  sandstone  come  under  the 
heads  of  building  stones,  glass  sand,  and  iron  ores.  These  are  des- 
cribed here  in  general  only,  all  details,  exact  locations,  etc.,  being 
given  in  subsequent  pages. 

The  Madi&on  sandstone,  in  the  vicinity  of  Madison,  yields  a  buif- 
colored  calcareous  sandstone  which  is  largely  quarried  and  used  for 
building  in  that  vicinity.  This  rock  contains  about  ten  per  cent,  of 
the  carbonates  of  lime  and  magnesia,  is  easily  cut,  and  obtainable  in 
large  blocks.  It  has  a  very  pleasing  appearance  in  the  fresh  state, 
but  has  some  tendency  to  darken  and  become  blotched  under  the  ac- 
tion of  the  weather.  The  same  rock  is  opened  upon  at  Middleton, 
Wis.  SUK.  — 35. 


546  GEOLOGY  OF  CENTRAL  WISCONSIN. 

and  in  one  or  two  places  in  the  town  of  Westport,  Dane  county, 
and  probably  exists  in  considerable  quantity  in  the  country  about 
Lake  Mendota.  The  peculiar  phase  which  yields  the  Madison  build- 
ing stone  is,  however,  local,  and  quite  inconstant.  More  commonly 
the  formation  is  made  up  of  white  and  brown  friable  sandstone,  nearly 
or  altogether  without  calcareous  admixture.  The  brown  layers  are 
occasionally  quite  ferruginous  and  firm,  yielding  a  fair  quarry  stone. 
The  white  sandstone  is  frequently  a  loose,  white,  purely  silicious  sand, 
and  would  be  of  considerable  value  for  glass  making.  In  one  place 
on  the  western  side  of  the  town  of  Honey  Creek,  the  Madison  sand- 
stone has  a  very  unusual  character,  containing  layers  of  a  much  indu- 
rated, fine-grained,  smooth-faced,  pink-tinted  rock  of  very  pleasing 
appearance. 

The  Mendota  limestone  is  more  frequently  quarried  than  the  Mad- 
ison sandstone.  It  is  not  anywhere  burnt  into  lime,  being  usually 
too  impure,  and  always  too  dark  colored,  but  the  heavy  yellow  layers 
that  characterize  some  ten  to  15  feet  of  its  middle  portions,  are  to  be 
seen  in  scores  of  quarries,  most  numerously  along  the  Wisconsin 
valley.  These  layers  yield  a  very  regular  stone,  of  any  thickness 
from  a  few  inches  to  two  or  three  feet,  which  is  commonly  used  for 
flagging  or  foundations,  but  occasionally  for  constructing  entire  build- 
ings. The  mill  at  Cambria,  Columbia  county,  is  built  of  rock  from 
the  Mendota  horizon. 

The  Potsdam  sandstone  itself  is  generally  altogether  too  friable  to 
be  used  as  a  building  material.  At  numbers  of  points  in  the  Baraboo 
valley,  however,  a  firm,  fine-grained,  white  rock  is  obtained  in  large 
blocks.  A  similar  rock  is  quarried  on  several  of  the  isolated  bluffs 
in  Juneau,  Adams  and  Jackson  counties,  the  horizon  being  about  200 
to  300  feet  below  the  summit  of  the  series.  A  very  much  indurated, 
frequently  quite  coarse,  rock  is  obtained  at  a  still  lower  horizon  at 
Packwaukee,  Marquette  county,  near  Wautoma,  Waushara  county,  at 
Stevens  Point,  Portage  county,  near  Grand  Rapids,  "Wood  county,  and 
at  Black  River  Falls,  Jackson  county.  This  rock  is  very  regular  in 
bedding,  white  to  straw  colored,  and  makes  a  very  durable  and  sightly 
building  stone. 

Limonite  iron  ores,  of  good  quality,  and  in  sufficient  quantity  to 
run  two  small  blast-furnaces,  occur  in  connection  with  the  Lower 
sandstone  in  Sauk  and  liichland  counties,  just  west  of  the  limit  of 
the  Central  Wisconsin  district.  Within  that  district,  the  only  ore  ob- 
served in  any  promising  quantity  occurs  in  the  upper  layers  of  the 
high-level  sandstone  that  flanks  the  quartzite  range  in  the  eastern 
part  of  the  town  of  Westfield,  Sauk  county.  Here,  at  a  number  of 


THE  LOWER  SILURIAN  ROCKS.  547 

points  several  miles  apart,  this  sandstone  may  be  seen  very  highly 
charged  with  the  brown  iron  oxide,  which,  at  times,  almost  entirely 
excludes  the  sandstone,  having  then  mingled  with  it  much  of  the  red 
or  anhydrous  oxide.  It  appears  quite  probable  that  the  amount  of 
merchantable  ore  to  be  obtained  in  this  neighborhood  is  sufficient  to 
warrant  exploitation.  Yery  ferruginous  sandstone,  at  a  similar  ho- 
rizon, occurs  at  other  points  along  the  Baraboo  ranges,  but  nowhere 
else  have  promising  indications  been  observed. 

THE  LOWER  MAGNESIAN  LIMESTONE. 

Succeeding  the  uppermost  layer  of  the  Potsdam  series,  the  Madi- 
son sandstone,  is  a  very  persistent  and  wide  spread  bed  of  magne- 
sian  limestone,  to  which  Owen  gave  the  name  of  Lower  Magnesian, 
to  distinguish  it  from  another  equally  persistent,  and  in  many  respects 
quite  similar,  magnesian  limestone,  that  occurs  higher  in  the  series. 
To  the  latter  the  name  Galena  limestone  has  since  become  attached, 
whilst  no  other  designation  lias  been  given  to  the  lower  formation. 
In  neither  case  can  the  term  magnesian  be  regarded  as  at  all  dis- 
tinctive, since  almost  all  of  the  limestone  beds  of  Wisconsin,  including 
the  whole  of  the  great  thickness  belonging  to  the  Niagara  group,  are 
highly  magnesian,  the  only  exception  to  the  general  rule  being  the 
Blue  limestone  of  the  Trenton  group.  There  appears  to  be  but  little 
doubt  that  the  Lower  Magnesian  is  nearly  the  exact  equivalent  of 
the  Calcifcrous  Sandrockof  New  York  and  Canada,  with  which  form- 
ation, indeed,  it  is  nearly  continuous  through  the  northern  peninsula 
of  Michigan  and  Canada  West. 

The  surface  extent  of  the  Lower  Magnesian  limestone  in  Central 
Wisconsin  is  not  nearly  so  great  as  that  of  the  Lower  sandstone,  being, 
in  all,  not  more  than  about  75  square  miles.  The  main  belt  occupied 
by  the  formation  enters  Columbia  county  on  the  northeast  ,with  a 
width  of  about  6  miles,  and,  spreading  further  and  further  west  as  it 
is  followed  southward,  occupies  much,  or  all,  of  the  towns  of  Randolph, 
Scott,  Springvale,  Courtland,  Lowville,  Otsego,  Fountain  Prairie, 
Columbus,  Hampden,  Leeds,  Arlington,  Lodi,  and  West  Point  in 
Columbia  county,  and  large  portions  of  lioxbury,  Berry,  Dane, 
Springfield,  Vienna,  Westport,  Windsor,  Bristol  and  York,  in  Dane 
county.  Still  further  south,  again,  the  formation  occurs  only  in  nar- 
row areas,  crowning  the  summits  of  the  ridges  bet\veen  the  valleys  in 
which  run  the  several  head  streams  of  the  Catfish  river,  or  forming 
narrow  strips  between  the  low  ground  of  the  valley  of  that  stream, 
and  the  higher  country  which  on  each  side  is  occupied  by  the  St. 


54:8  GEOLOGY  OF  CENTRAL  WISCONSIN. 

Peters  standstone,  and  Trenton  limestone.  On  the  southern  side  of 
Dane  county  the  Lower  Magnesian  sinks  to  the  level  of  the  Catfish 
valley,  spreading  over  a  considerable  area  in  the  towns  of  Rutland, 
Dunn,  Pleasant  Springs  and  Dunkirk.  The  numerous  narrow  steep- 
sided  valleys,  tributary  to  the  valley  of  Sugar  river,  in  Primrose, 
Springdale  and  Cross  Plains,  and  the  valley  of  Sugar  river  itself  in 
Verona  and  Montrose,  cut  down  to  the  upper  surface  of  the  Lower 
Magnesian,  which  thus  forms  narrow  strips  along  their  bottoms. 

Along  the  edge  of  the  main  area,  in  Columbia  county,  and  north- 
western Dane,  and  usually  not  more  than  two  or  three  miles  west  or 
north  from  it,  though  occasionally  more  than  this,  are  many  small 
isolated  bluffs  crowned  by  the  Lower  Magnesian.  These  vary  in  area 
from  a  few  acres  to  three  or  four  square  miles.  North  of  the  Wis- 
consin river  and  along  the  west  side  of  Sank  county,  as  far  as  the 
southern  side  of  the  Baraboo  valley,  the  Lower  Magnesian,  in  areas 
of  varying  size,  occupies  all  the  higher  ground,  the  country  being 
characterized  by  numerous  narrow  ridges,  with  intervening  narrow 
valleys.  North  of  the  Baraboo,  in  northwestern  Sauk  county  and 
southwestern  Juneau,  the  Lower  Magnesian  occurs  only  in  rare  and 
very  small  cappings  on  the  highest  ground. 

The  topographical  characters  of  the  regions  occupied  by  the 
Lower  Magnesian  differ  much,  according  as  they  occur  within  or 
without  the  drift-bearing  area,  and  also  according  to  whether  the 

O  f  o 

formation  exists  on  the  higher  grounds  only,  or  has  sunk  down  to  the 
lowest  levels.  All  of  these  regions,  however,  are  alike  in  possessing 
a  most  excellent  soil,  the  Lower  Magnesian  area  including  the  best 
agricultural  land  in  the  district.  In  Columbia  county  the  formation 
occupies  a  region  which  is  for  the  most  part  very  fertile,  high,  rolling 
prairie,  the  prairie  areas  forming  a  nearly  continuous  belt  from  the 
towns  of  .Scott  and  Randolph,  in  Columbia  county,  southwestward  to 
Middleton,  in  Dane  county.  This  high  belt  breaks  down  suddenly  to 
the  westward,  but  the  escarpment,  though  quite  bold,  is  without  the 
great  cliff-like  exposures  so  characteristic  of  the  Lower  Magnesian  as 
it  appears  along  the  lower  Wisconsin  and  upper  Mississippi  rivers. 
The  same  is  true  of  the  sides  of  the  limestone  ridges  about  the  heads 
of  the  Cattish  river.  Along  the  Wisconsin,  however,  below  Sauk 
City,  the  Lower  Magnesian  crowns  the  river  bluffs  often  with  bold 
cliffs,  the  difference  being  chiefly  due  to  the  absence  of  drift  materials. 
Along  the  western  side  of  Sauk  county,  the  drift  is  also  absent,  and 
the  usual  abrupt,  ridgy  topography  of  the  driftless  regions  is  every- 
where apparent,  the  limestone  capping  to  the  ridges  being  often  a  mero 
crest  of  rock,  large  fallen  masses  from  which  dot  the  side-hills  below. 


THE  LOWER  SILURIAN  ROCKS.  549 

AVliilst  in  minor  details  the  Lower  Magncsian  varies  much  as  to  its 
lithologicai  characters  —  even  individual  horizons  not  showing  any 
great  constancy  in  this  regard  —  all  parts  of  it  have  some  features  in 
common,  which  serve  to  distinguish  it  from  the  newer  limestone 
formations  of  the  region.  In  general,  it  may  be  said  that  the  Lower 
Magnesian  is  a  rnagnesian  limestone,  varying  in  composition  from 
varieties  that  contain  not  more  than  one  or  two  per  cent,  of  insoluble 
ingredients,  to  those  that  are  for  the  most  part  sand.  An  analysis 
has  been  given,  a  few  pages  back,  of  one  of  the  purest  phases,  whilst 
in  the  detailed  descriptions  of  this  chapter,  numerous  determina- 
tions of  the  quantity  and  nature  of  the  insoluble  ingredients  of 
both  pure  and  impure  varieties  will  be  found.  These  in  the 
purer  kinds  are  exceedingly  fine  and  clay-like,  whilst  in  the  less 
pure  they  are  usually  quartz  sand  of  varying  degrees  of  fineness, 
the  constituent  grains  always  much  rolled.  The  analysis  above 
cited,  as  also  others  made  for  the  survey,  do  not  show  the  car- 
bonates of  calcium  and  magnesium  in  the  right  proportion  to  make 
a  true  dolomite,  the  first-named  carbonate  being  always  in  excess. 
Older  analyses  show  a  nearer  approach  to  the  composition  of  dolomite. 
The  purest  kinds  have  usually  a  grayish-white  color,  a  minutely  crys- 
talline texture,  and  marked  conchoidal  fracture.  More  commonly  the 
white  back-ground  is  blotched  with  yellow,  whilst  other  layers  again 
occur,  in  which  the  buff  color  is  uniform.  These  are  usually  charac- 
terized by  a  close,  even,  granular  texture,  which  may  be  due  to  an 
admixture  of  sand  grains,  or  may  characterize  a  quite  pure  lime- 
stone. 

The  bedding  of  the  Lower  Magnesian  varies  much.  Usually  those 
layers  from  40  to  60  feet  above  the  base  are  the  heaviest,  the  indi- 
vidual layers  running  sometimes  to  a  thickness  of  4  to  6  feet,  whilst 
the  bedding  lines  are  exceedingly  indistinct.  In  the  upper  and  lower 
portions  of  the  formation,  the  layers  are  usually  much  thinner,  and 
more  distinct,  although  commonly  quite  irregular,  very  rough- sur- 
faced and  internally  porous,  with  drusy  cavities  that  are  lined  with 
calcite  and  dolomite  crystals.  Occasionally,  however,  the  lower  layers 
are  exceedingly  regular,  being  obtainable  in  large,  smooth-surfaced, 
compact,  and  finely  granular  slabs.  Highly  concretionary  layers,  some 
of  which  appear  even  to  have  a  brecciated  structure,  occur  at  many 
different  horizons  in  the  formation,  the  structure  sometimes  affecting 
in  the  highest  degree  a  layer  not  more  than  a  foot  thick,  whilst  above 
and  below,  for  many  feet,  no  trace  of  a  concretionary  structure  is  ap- 
parent. In  other  cases  much  greater  and  less  well-defined  thicknesses 
are  affected  in  this  manner.  One  of  the  most  prominent  features  of 


550  GEOLOGY  OF  CENTRAL  WISCONSIN. 

the  formation  is  the  rough-weathering  seen  on  nearly  all  outcrops,  in 
some  cases  due  to  the  concretionary  structure  of  the  rock. 

Chert  occurs  very  abundantly  throughout  the  Lower  Magnesian, 
and  of  three  or  four  different  kinds.  In  many  places  above  the  Mad- 
ison sandstone  there  is  to  be  seen  a  thin  layer  of  greensand,  and  above 
this  a  thinner  one,  one  to  ten  inches  in  thickness,  of  a  pure  white, 
oolitic,  chert,  which,  on  examination  under  the  microscope,  appears 
to  consist  of  egg-shaped  aggregations  of  fine  glassy  quartz  grains,  em- 
bedded in  a  still  finer  silicious  matrix.  This  layer  is  very  persistent, 
in  the  country  about  Madison.  A  sample  from  the  Madison  quarries 
yielded:  silica,  98.01;  alumina,  0.52;  iron  peroxide,  0.73;  lime,  0.67; 
magnesia,  0.21;  water,  0.24=:100.38.  The  same  oolitic  chert  occurs 
disseminated  through  the  layers  of  limestone  in  the  lower  beds,  to  the 
whole  mass  of  which  it  often  gives  the  appearance  of  an  oolitic  struc- 
ture. The  older  writers  on  Wisconsin  geology  all  speak  of  oolitic 
limestone  as  characterizing  the  lowest  portions  of  the  Lower  Magne- 
sian; so  far  as  my  observation  goes,  the  limestone  is  not  oolitic  itself, 
but  carries  disseminated  oolitic  chert.  Higher  up,  beginning  usually 
some  30  feet  above  the  Madison  sandstone,  a  more  compact  chert 
comes  in,  increasing  in  quantity  as  the  formation  is  traced  upward. 
This  chert  is  either  quite  compact  and  flinty,  occurring  in  irregular  lay- 
ers or  nodules,  or  is  more  or  less  cavernous,  the  cavities  being  lined 
with  drusy  quartz.  Associated  with  the  greyish-white  beds  of  the 
least  silicious  limestone,  is  a  chert  occurring  in  well-marked  layers 
and  rows  of  nodules,  which,  in  external  shape  and  soft  silicious  coat- 
ing, resemble  closely  the  flints  of  the  Chalk,  whilst  within  they  are 
often  beautifully  banded  and  jasper-like.  Still  higher  in  the  forma- 
tion, about  100  feet  above  its  base,  the  thin  layers  of  limestone  are 
often  replaced  bodily,  for  considerable  thicknesses,  by  a  compact  iron- 
stained  chert. 

Black  dendritic  markings  are  very  common  in  the  Lower  Mag- 
nesian, but  occur  in  the  greatest  abundance  and  beauty  in  those  layers 
that  are  fine-granular  and  buff-colored,  and  not  more  than  30  to  40 
feet  above  the  upper  surface  of  the  Madison  sandstone.  The  mineral 
causing  these  markings  is  supposed  to  be  the  black  oxide  of  man- 
ganese. 

In  stratigraphical  arrangement,  the  Lower  Magnesian  appears 
to  show  but  little  persistent  regularity.  An  attempt  to  make  out  a 
thoroughly  reliable  and  detailed  scheme  of  the  stratigraphy  of  this 
formation,  meets  with  two  considerable  difficulties.  The  first  of  these 
lies  in  the  fact  that,  although  exposures  are  very  numerous,  it  is  only 
rarely  that  any  considerable  thickness  can  be  seen  at  one'  place;  so 


THE  LOWER  SILURIAN  ROCKS.  551 

that  numerous  small,  often  somewhat  distant,  exposures  have  to  be 
thrown  into  place  by  means  of  aneroid  observations,  a  not  very  satis- 
factory guide.  The  other  difficulty  arises  from  the  irregular  nature 
of  the  upper  surface  of  the  formation,  which  is  due  to  erosion  before 
the  deposition  of  the  St.  Peters  sandstone,  and  as  a  result  of  which 
the  Lower  Magnesian  varies  from  50  to  250  feet  in  thickness.  From 
this  it  follows  that  all  determinations  of  horizon  within  the  Lower 
Magnesian,  made  by  measuring  from  the  base  of  the  St.  Peters  sand- 
stone downwards,  are  worthless.  Varying  so  greatly  as  it  does  in  thick- 
ness, beds  immediately  underneath  the  St.  Peters  may,  in  fact,  be 
nearer  the  base  than  the  summit  of  the  formation. 

In  the  region  around  Madison,  the  Lower  Magnesian  has  usually  a 
thickness  of  about  TO  to  80  feet,  though  it  may  run  from  50  to  100. 
feet,  The  following  outline  scheme  of  the  succession  of  its  layers  in 
this  region  is  an  abridgement  of  a  more  elaborate  one,  which  ac- 
companied the  annual  report  on  the  field  work  of  1874,  to  which  was 
also  attached  a  large  chart  of  grouped  sections.  These  are  not  here 
reproduced,  because  the  work  of  later  seasons  proved  them  to  have 
only  a  local  value.  The  numbers  in  the  scheme  are  from  below 
upwards,  on  account  of  the  uncertainty  as  to  any  measurements  from 
above,  downwards.  The  exposures  cited  are  only  single  instances  out 
of  many  representing  the  different  layers. 

Ft.    In. 
VII.  Concretionary,  brownish-yellow  layers,  which  at  times  are  quite  sandy, 

and  at  others  contain  not  more  than  3  to  4  per  cent  of  fine  aluminous 
impurities;  Veerhusen's  quarry,  Sec.  25,  Westport;  Williams'  quarry, 
Sec.  38,  Madison.  Tliickness  about 10 

VI.  Heavy,  indistinctly  bedded  layers,  which  appear  to  vary  much  in  charac- 
ter, being  sometimes,  as  at  Williams'  quarry,  Sec.  33,  Madison,  greyish- 
white,  nearly  free  from  foreign  ingredients,  minutely  crystalline,  con- 
choidal-fracturing  and  compact,  but  with  small  cavities  lined  with  dolo- 
mite crystals.  Interstratified  are  continuous  seams,  and  rows,  of  white 
surfaced  nodules  of  jaspery  chert.  At  other  times,  as  at  Veerhusen's 
quarry,  Sec.  25,  Westport,  these  layers  have  a  greenish-tinted  buff  color, 
and  a  fine-granular  texture,  containing  30  to  40  per  cent,  of  fine  quartz 

sand,  and  little  or  no  chert.    Thickness,  in  all,  about 15 

V.  Thin,  regularly  bedded,  greenish  yellow,  fine-granular  layers,  with  very 
abundant  and  large  dendritic  markings;  Veerhusen's  quarry 10 

IV.  Very  irregularly  bedded,  alternatingly  heavy  and  thin,  white-and-yel- 
low- mottled,  rough-textured,  very  cherty,  layers;  Middleton  quarry. ...  20 

III.  Thin,  irregular,  usually  somewhat  sandy,  brownish  layers,  including  oc- 
casionally beds  of  1  to  2  feet  in  thickness.  Near  the  top  a  very  highly 
brecciated  layer,  1  foot  thick,  often  comes  in  (quarry  near  the  school 
house,  Middleton);  wliilst  below,  oolitic  chert  pervades  the  limestone,  and 
alternations  of  more  and  less  sandy  layers  occur,  constituting  a  passage 
downwards  into  the  Madison  sandstone  (Middleton  and  Madison  quar- 
ries). In  some  cases  this  gradation  is  not  marked,  the  transition  from  a 


552  GEOLOGY  OF  CENTRAL  WISCONSIN. 

nearly  pure  limestone  to  a  nearly  non-calcareous  sandstone  being  quite   Ft.   In. 
abrupt  (cut  on  Chicago  and  Northwestern  road,  Sec.  35,  Madison;  also, 

cut  on  same  road  at  Mendota  Station,  Westport).    Thickness 15 

II.  White  oolitic  chert  layer  (Madison  quarries) 6 

I.  Greensand  layer  (Madison  quarries) 6 

Total . .  71 


The  bold  bluff  that  rises  from  the  mouth  of  Honey  creek,  Sauk 
county,  has  already  been  cited  as  giving  an  unusually  complete  sec- 
tion of  the  upper  part  of  the  Potsdam  series.  It  shows,  also,  the 
largest  continuous  exposure  of  the  Lower  Magnesian  that  I  have  ever 
seen  —  a  vertical  cliff  over  50  feet  in  height.  The  following  is  a  de- 
tailed section  of  this  cliff,  beginning  above: 

Ft.    In. 

1.  Heavy  layer  of  brown- and-yellow-mottled  limestone,  which  leaves  on  solu- 

tion 2.2  per  cent,  of  very  fine  clayey  residue 1 

2.  No  good  exposure 5     . . 

3.  Heavy  layer  of  very  close-textured,  nearly  white,  limestone,  with  many 

dendritric  markings;  residue  9.09  per  cent,  and  clayey 1      2 

4.  Thin  layers,  3  to  4  inches  each,  of  limestone  like  the  last;  residue  5.8  per 

cent.,  clayey 3     .. 

5.  Thin  layers  of  brown-and-gray-mottled  limestone  with  minute  crystal-lined 

cavities;  residue  2.9  per  cent.,  clayey 6 

6.  Heavy  layer  of  light  gray,  close-textured  limestone,  with  cavities  like  No. 

5;  residue  8.35  per  cent.,  clayey 3      6 

7.  Two  heavy  layers  like  No.  6;  residue  6  per  cent.,  clayey 5      2 

8.  Shaly  layers  of  porous,  yellow- and-gray-mottled,  crystalline  limestone; 

residue  7-2  per  cent.,  clayey 2      3 

9.  Three  layers  of  yellow-and-gray-mottled,  close-textured  limestone;  residue 

18.85  per  cent.,  clayey 3 

10.  Heavy  layer  of  yellowish,  sandy  limestone;  residue  40.17  per  cent.,  fine, 

gray  sand 2 

11.  Heavy  non- arenaceous  layer,  with  very  indistinct  subordinate  bedding 3        6 

12.  Very  irregular,  brownish,  close-textured  Limestone,  occurring  in  thin  broken 

layers,  the  cracks  being  lined  with  white  stalactitic  lime  carbonate;  resi- 
due 4.38  per  cent.,  clayey 1      6 

13.  Two  heavy  layers  of  brownish- gray,  close- textured  limestone;  residue  3. 42 

per  cent.,  clayey 2      6 

14.  Irregularly  thin  bedded,  very  close- textured  chonchoidal- fracturing  gray 

limestone;  residue  9.3  per  cent.,  clayey 1      4 

15.  Very  indistinctly  bedded,  nodular- weathering,  close-textured,  mottled  lime- 

stone; residue  7 . 17  per  cent.,  clayey 8      8 

16.  Very  irregularly  bedded,  rough-surfaced,  close-textured,  gray  limestone; 

residue  28.97  per  cent.,  fine  sand  and  clay 3      6 

17.  Thick  layer  of    porous,  brecciated,  highly-crystalline  limestone;  residue 

13 .67  per  cent.,  fine  sand  and  white  clay 1      9 

18.  Thick  layer  of  compact,   yellowish  brown,  granular,   smooth-fracturing 

Limestone,  with  much  dendritic  manganese  oxide;  residue  16.65   per 

cent.,  clayey 1      7 

Total . .  52      5 


THE  LOWER  SILURIAN  ROCKS.  553 

The  foot  of  the  cliff  is  evidently  very  close  to  the  top  of  .the  Mad- 
ison sandstone,  whose  first  exposure,  however,  is  15  feet  below.  Al- 
though the  foreign  impurities  increase  slightly  in  quantity  down- 
wards, we  find  no  distinct  evidence  of  a  gradation  into  the  sandstone 
below.  In  fact  the  whole  cliff  shows  a  nearly  uniform  material,  the 
differences  being  but  slight  between  the  several  layers. 

North  of  Dane  county  the  Lower  Magnesiau  has  the  same  general 
characters  as  described,  with  some  local  variations;  but  no  scheme  of 
elementary  stratification  for  these  districts  has  been  made  out.  In 
the  high  prairie  country  of  southern  Columbia  county  the  formation 
attains  a  thickness  of  120  to  140  feet  or  more,  the  highest  beds  being 
generally  very  cherty,  or  even  replaced  bodily  by  chert.  In  central 
and  northern  Columbia  the  lowest  layers  have  lost  their  irregularity 
of  bedding  and  rough- texture,  and  have  become  very  evenly  be.dded 
and  closely  granular,  at  the  same  time  showing  little  or  no  sandy  ad- 
mixture, and  no  passage  downwards  into  the  Madison  sandstone, 
which  itself  continues  non-calcareous  upwards  to  contact  with  the 
Lower  Magnesian.  Along  the  western  side  of  the  district,  in  west- 
ern Sauk  county,  the  same  lack  of  gradation  downwards  is  generally 
to  be  noticed.  In  a  large  region  lying  south  of  the  Baraboo  quartz- 
ite  ranges,  small  pebbles  of  red  quartzite  are  frequently  found  in  the 
Lower  Magnesian. 

The  irregular  upper  surface  of  the  Lower  Magnesian,  already 
mentioned,  is  one  of  the  most  striking  features  of  the  formation. 
The  first  demonstration  of  the  existence  of  such  an  eroded  surface  was 
made  by  Prof.  Chamberlin,  in  eastern  Wisconsin,  but  since  then 
numerous  confirming  facts  have  been  collected  in  other  parts  of  the 
state.  The  valley  of  Sugar  river,  and  its  numerous  branch  ravines,  in 
the  towns  of  Verona,  Montrose,  Primrose,  Springdale  and  Cross 
Plains,  cut  down  to  the  Lower  Magnesian,  the  St.  Peters  sandstone 
forming  the  steep  valley  sides.  At  numerous  points  in  these  valleys, 
exposures  of  the  Lower  Magnesian  are  found  at  higher  levels  than 
those  of  the  St.  Peters,  and  under  such  circumstances  that  they  can- 
not be  regarded  as  proving  a  distinct  and  hitherto  unrecognized  layer 
of  limestone;  for  they  are  often  near  to  large  sandstone  ledges,  which 
rise  continuously  from  lower  to  higher  levels  than  those  at  which  the 
limestone  is  seen.  A  still  more  striking  proof  is  found  in  the  patches 
of  St.  Peters  sandstone  that  are  to  be  seen  lying  directly  in  the  hol- 
lows of  the  Lower  Magnesian,  in  the  southern  part  of  the  town  of 
Arlington,  Columbia  county;  whilst  the  evidence  is  perhaps  even 
stronger  in  the  case  of  Gribralter  Bluff,  in  the  town  of  West  Point, 
Colnrnbia  county,  where  a  vertical  cliff  135  feet  high,  of  St.  Peters 


554  GEOLOGY    OF   CENTRAL  WISCONSIN. 

sandstone,  has  its  base  40  to  60  feet  lower  than  the  exposures  of  Lower 
Magnesian  in  the  immediate  vicinity.  About  Madison,  in  Danecoun 
ty,  the  Lower  Magnesian  is  only  from  50  to  80  feet  thick;  just  north 
in  the  high  prairie  country  on  the  borders  of  Columbia  and  Dane 
counties,  it  has  thickened  to  125  to  140  feet,  a  fact  in  itself  sufficient 
to  suggest  the  existence  of  an  eroded  upper  surface.  It  is  not  improb- 
able that  some  of  the  swells  of  this  high  region  are  directly  due  to 
the  irregular  surface  of  the  underlying  limestone. 

The  fossils  of  the  Lower  Magnesian  are  not  common,  and  when 
found  are  but  obscure  gasteropod  and  orthoceratite  markings  in  the 
chert  of  the  uppermost  layers.  If  the  two  small  patches  of  limestone 
already  alluded  to  as  occurring  in  the  region  between  the  quartzite 
ranges  of  the  Baraboo  be  regarded  as  belonging  to  this  formation, 
quite  an  interesting  addition  is  to  be  made  to  the  hitherto  meager 
list  of  Lower  Magnesian  forms.  The  limestone  of  one  of  these  small 
areas  has  yielded  a  number  of  fossils  which  are  regarded  bv  Mr.  R. 

t/  O  t/ 

P.  "Whitficld,  as  "  certainly  not  lower  than  the  Lower  Magnesian,"  to 
which  formation  the  composition,  lithological  character,  and  position 
of  the  rock  would  also  refer  them,  the  difficulty  lying  in  the  pecu- 
liar conclusions  that  are  thus  led  to  with  regard  to  the  Lower  sand- 
stone in  the  vicinity,  as  explained  on  a  previous  page.  These  fossils 
are:  Stromatopora,  und.  sp. ;  Orthis  Barcibuensis?  ;  Ilolopea,,  n. 
sp. ;  Maclurea  Swezeyi,  n.  sp. ;  Illcenus  antiquatus,  n.  sp. ;  Dicello- 
cephaliis  Barabuensis,  n.  sp.;  D.  Eatoni,  n.  sp. ;  and  triangular 
sheath-like  bodies. 

The  economic  contents  of  the  Lower  Magnesian  are  limestone  for 
burning  into  lime,  and  building  stone.  Galena,  in  small  quantities, 
lias  been  obtained  from  crevices  in  the  Lower  Magnesian,  but  the 
only  occurrence  of  this  kind  known  in  Central  Wisconsin  is  that  near 
Doylestown,  in  Columbia  county,  where  a  limited  crevice  in  the  lower 
part  of  the  formation  has  yielded  several  hundred  pounds  of  this  ore. 
This  occurrence  is  interesting  because  at  such  a  distance  from  the 
productive  lead  region.  I  have  seen  no  other  indication  that  the 
Lower  Magnesian  is  ore-bearing.  Lime  is  burnt  from  the  Lower 
Magnesian  at  a  great  many  points,  and  from  quite  different  horizons. 
The  lime  produced  is  uniformly  quite  slow  in  slacking,  making,  how- 
ever, a  very  strong  mortar.  It  is  rarely  very  white.  Many  of  the 
lower  beds  are  too  sandy  for  lime  burning,  the  best  for  the  purpose 
being  apparently  the  heavy  grayish-white  layers  40  to  50  feet  above 
the  Madison  sandstone.  Twenty  thousand  bushels  annually  are  burnt 
from  these  layers,  on  Sec.  33,  T.  7,  R.  9  E.,  the  product  being  widely 
known  as  "  Madison  lime."  The  Lower  Magnesian  is  in  general  too 


THE  LOWER  SILURIAN  ROCKS.  555 

roughly  or  too  indistinctly  bedded  to  make  good  building  stone,  but 
the  heavy  beds  just  alluded  to  sometimes  take  on  a  different  character, 
becoming  fine-granular,  and  very  evenly  bedded,  and  yielding  a 
superior  cream-colored  stone.  Such  a  stone  is  quarried  at  one  or  two 
points  in  the  town  of  West.port,  and  has  been  used  in  the  construction, 
of  the  State  Hospital  for  the  Insane,  and  the  United  States  Court 
House  at  Madison. 

THE  UPPER  OR  ST.  PETERS  SANDSTONE. 

To  the  layer  of  sandstone  which,  everywhere  in  Wisconsin,  Iowa  and 
Minnesota,  is  found  resting  upon  the  eroded  surface  of  the  Lower 
Magnesian,  Dr.  Owen  gave  the  name  of  "Upper"  sandstone,  to  dis- 
tinguish it  from  the  "  Lower  "  or  Potsdam  sandstone.  He  also  desig- 
nated it  as  the  "  St.  Peters  "  sandstone,  from  its  prominent  exposures 
on  the  St.  Peters  river  in  Minnesota.  Mr.  Hall  regards  the  St.  Peters 
sandstone  as  the  equivalent  of  the  Chazy  limestone  of  ]S"ew  York,  on 
account  of  its  strati  graphical  position.  As  to  the  correctness  of  this 
reference,  I  have  not  the  means  of  forming  an  accurate  opinion;  cer- 
tainly, however,  between  the  periods  of  deposition  of  the  Lower  Mag- 
nesian and  St.  Peters,  there  was  a  long  gap,  whose  record  is  found  in 
the  eroded  surface  of  the  first-named  formation. 

For  a  purely  silicious  sandstone,  and  one  only  20  to  100  feet  in 
thickness,  the  St.  Peters  has  an  extraordinarily  wide  distribution. 
It  is  known  in  Wisconsin  at  points  250  miles  apart  from  east  to  west, 
and  180  from  south  to  north,  whilst  to  the  west,  south  and  east  it  ex- 
tends far  beyond  the  limits  of  the  state.  In  the  last  named  direction 
it  is  known  to  extend,  because  a  number  of  Artesian  wells  at  points 
along  the  shore  of  Lake  Michigan  show  it  with  an  unusual  thickness. 
To  the  westward,  in  Minnesota,  it  is  recognized  for  an  additional  dis- 
tance of  at  least  100  miles,  whilst  to  the  southward  also  it  is  known 
to  extend  100  miles  beyond  the  Wisconsin  line.  Throughout  all  this 
large  region,  there  is  no  question  whatever  of  the  identity  of  the 
formation,  or  of  its  actual  continuity.  Moreover,  as  far  south  as  Mis- 
souri, the  St.  Peters  is  in  all  probability  represented  by  the  upper- 
most of  the  alternations  of  sandstone  and  limestone  that  form  a  large 
portion  of  the  Lower  Silurian  strata  of  that  section.  Thus  it  appears 
that  a  nearly  purely  silicious  sandstone  of  inconsiderable  thickness 
has  an  unbroken  extent  over  a  region  whose  diameters  are  500  and 
400  miles. 

In  the  Central  Wisconsin  district  the  St.  Peters  has  never  a  very 
wide  surface  extent,  forming  more  commonly  narrow  bands  around 
the  areas  of  the  Trenton  limestone.  It  is  wholly  confined  to  Colum- 


556  GEOLOGY  OF  CENTRAL  WISCONSIN. 

bia  and  Dane  counties.  In  the  former,  it  is  met  with  in  the  north- 
east corner  of  the  county,  in  the  towns  of  Randolph  and  Conrtland, 
with  a  thickness  of  only  20  feet,  and  forming  strips  not  more  than  a 
few  rods  wide  around  several  areas  of  Trenton  limestone.  Further 
south  its  main  area  lies  altogether  east  of  Columbia  county,  but  it  is 
found  again  in  the  southeastern  the  towns  of  Columbus  arid  Hamp- 
den,  with  the  same  small  thickness  and  distribution  in  a  narrow  belt 
around  an  area  of  Trenton  limestone.  The  St.  Peters  is  absent  every- 
where else  in  Columbia  county,  except  in  live  small  patches  on  the 
high  prairie  of  Arlington,  and  in  a  still  smaller  area,  but  with  a  thick- 
ness of  125  feet,  in  the  high  peak  known  as  "Gibralter  Bluff,"  in  the 
town  of  West  Point.  In  Dane  county,  the  St.  Peters  is  found  under- 
lying the  Trenton  on  both  sides  of  the  Catfish  valley,  sometimes 
coming  to  the  surface  as  a  narrow  band  only,  at  other  times  having 
quite  a  surface  spread,  as  in  Sun  Prairie,  Medina,  Cottage  Grove, 
Deerfield,  Fitchburg,  Oregon,  Montrose,  and  Verona;  these  larger 
areas  including  a  number  of  small  patches  of  Trenton  limestone, 
which  caps  the  summits.  On  the  west  side  of  Sugar  river,  though 
having  its  full  thickness,  the  St.  Peters  comes  to  the  surface  only  in 
narrow  bands,  forming  the  sides  of  deep  and  narrow  valleys.  The 
same  is  true  of  the  south  side  of  the  valley  of  Black  Earth  creek  in 
Cross  Plains  and  Middleton.  In  Berry,  Springfield,  and  northern 
Middleton,  the  St.  Peters  occurs  only  in  a  few  limited  areas  on  the 
highest  ground.  The  whole  surface  spread  of  the  St.  Peters,  in  Col- 
umbia and  Dane  counties,  is  not  more  than  225  square  miles,  all  but 
6  or  8  of  which  is  in  the  latter  county. 

In  eastern  Columbia  and  Dane  counties  the  St.  Peters  sandstone 
does  not  contribute  any  marked  topographical  features  to  the  coun- 
try, being  comparatively  thin  and  generally  drift  covered.  Where  it 
occurs  in  narrow  bands  around  the  Trenton  areas,  its  place  is  not  un- 
commonly marked  by  an  abrupt  change  of  level.  On  the  west  side  of 
Dane  county,  however,  and  especially  west  of  Sugar  river,  which 
forms  the  western  boundary  of  the  region  of  the  Glacial  Drift,  the  St. 
Peters  affects  the  scenery  of  the  country  in  a  marked  degree.  Here 
we  find  it  having  its  full  thickness  of  80  to  100  feet,  and  producing, 
by  its  friability,  abrupt,  and  not  infrequently  precipitous  and  rocky, 
valley  sides,  whose  summits  are  capped  by  the  Trenton  limestone, 
whilst  the  valley  bottoms  are  on  the  Lower  Magnesian.  In  the  val- 
leys themselves,  isolated  towerlike  rocks  of  the  St.  Peters  occur,  of 
varying  size,  and  occasionally  of  greater  area  at  top  than  at  bottom. 
Some  of  these  contain  the  full  thickness  of  the  St.  Peters,  and  are 
crowned  with  the  lowest  layers  of  the  Trenton. 


THE  LOWER  SILURIAN  ROCKS.  557 

The  St.  Peters  does  not  usually  much  affect  the  soil,  since  it  forms 
only  steep  side-hills,  or  else  is  buried  beneath  the  drift.  Occasion- 
ally, however,  where  it  comes  near  the  surface  over  small  level  areas, 
as  in  part  of  the  Sugar  river  valley,  in  the  town  of  Yerona,  it  pro- 
duces a  loose  sandy  soil. 

In  lithological  characters  the  St.  Peters  is  remarkably  uniform. 
So  far  as  my  observation  extends,  it  is  invariably  formed  of  a  fine, 
purely  silicious,  sand,  whose  constituent  grains  are  much  rolled.  No 
sign  of  crystalline  surfaces  to  the  grains  has  been  observed  in  the 
many  specimens  examined  with  the  microscope.  The  only  foreign 
materials  in  the  St.  Peters  are  the  hydrous  and  anhydrous  iron  oxides, 
which  occur  in  all  parts  of  the  formation,  banding  it,  or  staining  it 
for  great  thicknesses,  with  yellow,  brown,  or  red.  The  iron  oxide 
acts  as  a  cementing  material,  but  is  not  commonly  in  sufficient  quan- 
tity to  give  the  rock  any  considerable  coherence.  In  the  more  west- 
ern development  of  the  St.  Peters,  it  is  de-scribed  as  often  wholly  with- 
out the  iron  oxides,  and  made  up  of  pure  white,  entirely  incoherent, 
sand,  but  this  is  not  common  in  Central  Wisconsin.  Greensand  lay- 
ers, like  those  that  occur  in  the  Lower  sandstone,  are  found  also  in 
the  St.  Peters,  but  none  have  come  under  my  observation.  No  gra- 
dation downwards  or  upwards  into  the  adjacent  limestones  by  mingling 
with  calcareous  material  has  ever  been  noticed.  No  subordinate  divi- 
sion of  the  St.  Peters  sandstone  exists.  It  is  quite  uniform  in  char- 
acter throughout.  The  bedding,  however,  is  usually  distinct,  the  lay- 
ers being  ordinarily  very  heavy,  though  sometimes  quite  thin  and 
shaly.  The  lines  of  lamination  are  often  marked  by  a  red  and  white 
banding  when  no  planes  of  separation  can  be  detected.  The  surfaces 
of  large  exposures  frequently  show  the  hard,  vitrified  crust  so  charac- 
teristic of  the  Lower  sandstone.  To  this  induration  is  evidently  due 
the  maintenance  of  tower-like  forms  and  cliffs  in  so  friable  a  material. 

The  older  geologists  describe  the  St.  Peters  sandstone  as  very  uni- 
form in  thickness  placing  it  at  from  70  to  100  feet,  with  a  nearly 
constant  thickness  of  80  to  90  feet.  According  to  the  results  of  the 
present  survey,  although  such  constancy  probably  holds  true  for  south- 
western Wisconsin,  elsewhere  the  formation  is  exceedingly  variable 
in  this  regard.  On  the  east  side  of  the  Catfish  valley  it  is  50,  40  and 
20  feet  in  thickness.  Further  northeast  along  its  line  of  outcrop, 
Prof.  Chamberlin  has  found  it  but  a  few  inches  in  thickness,  and  then 
suddenly  expanding  to  80  or  100  feet.  The  same  irregularity  is  ob- 
served along  its  line  of  outcrop  to  the  Michigan  line. 

The  St.  Peters  has  been  reported  hitherto  as  entirely  barren  in  fos- 
sils, but  recently  a  few  have  been  found  in  the  Eastern  Wisconsin 


558  GEOLOGY  OF  CENTRAL  WISCONSIN. 

district.     No  traces  of  fossils  have  ever  been  observed  in  Central  Wis- 
consin. 

The  only  economic  contents  of  the  St.  Peters  are  to  be  found  in 
the  sand  of  which  it  is  made.  This  can  be  shoveled  out  and  used  for 
all  purposes  to  which  sand  is  ordinarily  applied.  Frequently  the 
sand  is  of  such  purity  and  whiteness  as  to  be  of  excellent  quality  for 
glassmaking,  but,  as  already  said,  this  phase  of  the  formation  is  more 
characteristic  of  its  development  in  the  western  part  of  the  state  and 
along  the  Mississippi. 

THE  TRENTON  LIMESTONE. 

In  Wisconsin  and  the  adjoining  portions  of  Minnesota,  Iowa  and 
Illinois,  the  St.  Peters  sandstone  is  succeeded  by  300  to  350  feet  of 
limestone  beds.  These  are  apparently  the  equivalents  of  the  Treaton 
series  of  New  York,  but  comprise  two  well  marked  members,  the  up- 
per one  of  which  has  no  exact  representative  among  the  eastern  rocks, 
whilst  the  lower  and  thinner  of  the  two,  as  indicated  by  its  numer- 
ous fossils,  represents  exactly  the  Birdseye  and  Black  river  limstone. 
To  this  lower  member  exclusively  it  has  become  customary  in  Wis- 
consin to  attach  the  name  of  Trenton,  the  upper  being  known  as  the 
"  Galena  "  limestone,  from  the  fact  that  it  is  the  main  repository  of  the 
lead  ores  of  the  Upper  Mississippi  lead  region.  This  nomenclature  is 
retained  in  the  present  report. 

In  the  Central  Wisconsin  district  the  Trenton  limestone  has  a  sur- 
face distribution  of  about  220  square  miles,  being  confined  wholly  to 
Dane  and  Columbia  counties.  In  the  latter  county  it  occurs  in  two 
principal  areas,  one  in  the  northeast  occupying  the  eastern  and  cen- 
tral parts  of  Randolph,  and  the  northeast  part  of  Court-land;  the 
other,  in  the  southeast,  covering  southern  Columbia  and  southeastern 
Hampden.  In  Dane  county  the  formation  has  a  much  wider  spread. 
In  the  towns  on  the  east  side  of  the  Catfish  valley  it  covers  all  the 
higher  grounds,  occurring  in  a  number  of  detached  areas  of  very  dif- 
ferent sizes.  Some  of  these  are  quite  small,  running  from  a  few  acres 
to  one  or  two  square  miles  in  extent,  as  in  Medina  and  Deerfield, 
where  they  are  very  numerous;  others,  however,  cover  the  greater 
part  of  a  township,  or  even  two  or  three  townships,  as  in  the  case  of 
the  large  one  which  occupies  nearly  all  of  Christiana  and  Albion,  with 
considerable  portions  of  Pleasant  Springs  and  Dunkirk.  On  the  west 
side  of  the  Catfish,  in  Rutland,  Oregon,  Fitchburg,  Verona  and  Mont- 
rose,  are  a  number  of  small  areas  of  Trenton,  occurring  as  isolated 
ridges  amidst  a  lower  country  occupied  by  the  St.  Peters.  A  large 


THE  LOWER  SILURIAN  ROCKS.  559 

area  of  Trenton  occupies  the  high  ground  at  the  head  of  Sugar  river, 
in  Cross  Plains  and  Middleton,  whilst  the  numerous  narrow  ridges 
"between  the  branch  streams  of  Sugar  river  in  Primrose  and  Spring- 
dale  are  everywhere  crowned  by  this  formation,  which  in  the  highest 
ridges  is  present  in  its  full  thickness.  The  high  Trenton  area  of 
Middleton  and  Cross  Plains  constitutes  the  divide  between  the  heads 
of  Sugar  river  and  Black  Earth  creek.  On  the  south  side  of  the  val- 
ley of  the  latter  stream  it  breaks  down  quite  suddenly.  Further 
north,  in  northwestern  Middleton,  southwestern  Springfield  and  south- 
ern Berry,  a  few  very  small  Trenton  areas  are  met  with. 

No  very  distinctive  topographical  characters  mark  the  region  occu- 
pied by  the  Trenton  limestone.  Most  commonly  the  areas  underlaid 
by  it  are  prairie  areas,  and  in  some  cases  the  coincidence  of  Trenton 
and  prairie  areas  is  striking.  In  all  cases  the  soil  derived  from  it  is 
very  fertile.  In  eastern  Dane  and  Columbia,  it  occupies  areas  of 
gently  rolling  to  level  country,  whilst  on  the  west  side  of  Dane  it 
forms  the  rounded  summits  of  steep  and  narrow  ridges.  Hardly  ever 
forming  natural  outcrops  of  any  size,  it  contributes  no  especially  pic- 
turesque features  to  the  scenery. 

The  lithological  characters  of  the  Trenton  limestone  contrast 
strongly  with  those  of  the  Lower  Magnesian,  it  being  throughout  very 
evenly  bedded,  commonly  close-textured,  rarely  cherty,  and  having 
aluminous  (clayey)  rather  than  silicious  (sandy)  impurities.  More- 
over, though  largely  dolomitic,  it  includes  a  considerable  thickness  of 
non-magnesian  limestone,  standing,  in  this  respect,  alone  amongst  the 
Silurian  limestones  of  the  northwest.  In  the  lead  region,  according 
to  Hall  and  Whitney,  only  the  lower  18  to  20  feet  of  the  Trenton  are 
dolomitic,  constituting  the  "Buff"  limestone  of  their  and  other  re- 
ports, whilst  above.,  all  of  the  remaining  50  to  80  feet  of  the  forma- 
tion are  true  limestone,  into  which  a  small  and  gradually  increasing 
amount  of  magnesia  enters  as  the  upper  layers  pass  into  the  overly- 
ing Galena.  The  lower  of  these  divisions,  the  Buff  limestone,  with  a 
thickness  of  25  feet,  is  well  marked  throughout  Columbia  and  Dane 
counties,  as  is  also  the  lower  portion  of  the  Blue  limestone  immedi- 
ately above.  The  higher  portions  of  the  formation,  which  have  for 
the  most  part  been  removed  by  denudation,  and  are  hence  but  rarely 
seen,  do  not  seem  to  bear  out  Hall's  and  Whitney's  descriptions,  since 
they  certainly  include  some  dolomitic  layers,  in  appearance  quite  like 
the  Buff  beds.  The  exposures  of  these  higher  beds  are,  however,  so 
infrequent,  that  I  would  advance  this  statement  with  some  doubt,  but 
for  the  fact  that  in  the  Eastern  Wisconsin  district,  where  all  parts  of 
the  formation  are  well  developed,  Professor  Chamberlin  has  made  out 


560  GEOLOGY  OF  CENTRAL  WISCONSIN. 

definitely  an  alternating  series,  all  the  beds  of  which  are  mao-nesian. 

.-  ~  O 

This  succession,  beginning  below,  is  as  follows:  Lower  Buff  (the 
"Buff"  of  the  Lead  Region),  dolomitic,  23  feet;  Lower  Blue,  also 
magnesian,  23  feet;  Upper  Buff,  dolomitic,  55  feet;  Upper  Blue, 
also  magnesian,  15  feet.  Only  the  two  lower  ones  of  these  are  ordi- 
narily seen  in  the  Dane  county  quarries. 

The  Buff  (or  Lower  Buff)  limestone  is  a  very  evenly  bedded,  bluish 
to  buff-colored,  close-textured  dolomite,  in  layers  from  a  few  inches 
to  2  or  3  feet  in  thickness.  Externally  the  layers  are  usually  a 
brighter  yellow  than  within,  owing  to  a  partial  peroxidation  of  the 
iron-protoxide  contained  in  the  rock.  The  following  analysis  is  one 
from  the  Buff  layers  only  a  short  distance  below  the  junction  with  the 
Blue,  from  Earth's  quarry,  in  the  southern  part  of  the  town  of  Bris- 
tol, Dane  county: 

Carbonate  of  lime 56*07 

Carbonate  of  magnesia , 35.32 

Silica 4.45 

Alumina 2.08 

Iron  sesquioxide 69 

Iron  protoxide^ 58 

Water..  .46 


99.65 

In  the  upper  part  of  the  Buff'  limestone,  purplish-brown,  close- 
textured,  conchoidal-fracturing  layers  occur,  which  contrast  much 
with  the  remainder  of  the  stratum.  The  Buff  limestone  yields  a  good 
building  stone  and  is  very  frequently  quarried. 

The  Blue  (Lower  Blue)  is  to  be  seen  ordinarily  only  in  its  lower 
half,  2  to  10  feet  of  which  are  not  unfrequently  laid  bare  in  quarries 
on  the  Buff  beds.  These  lower  layers  are  very  thin,  nodular- surfaced, 
and  made  up  of  dark  bluish-gray,  flinty-textured  limestone,  in  which 
small  specks  and  strings  of  calcite  are  thickly  scattered,  and  in  which 
also  numerous  fossil  fragments  are  imbedded.  Included  between 
these  layers  are  seams  of  a  very  thinly  and  regularly  laminated,  dark 
brown,  fragile,  calcareous  shale,  showing  numerous  black  graptolite- 
like  markings.  Of  the  following  analyses  of  the  Blue  limestone,  No. 
I  is  of  rock  taken  from  the  same  locality  as  the  Buff,  of  which  an 
analysis  has  just  been  given,  and  nearly  at  the  junction  of  the  two. 
Of  the  other  analyses,  added  for  comparison,  No.  II  is  cited  from  the 
report  of  Mr.  Moses  Strong  on  the  lead  region,  and  is  from  Sec.  36, 
T.  5,  R.  2  E.,  whilst  No.  Ill  is  of  Blue  limestone  from  near  Benton, 
on  the  Fever  river,  and  is  cited  from  J.  D.  Whitney's  report  on  the 
lead  region: 


THE  LOWER  SILURIAN  ROCKS.  561 

I. 

Carbonate  of  lime 84.02 

Carbonate  of  magnesia ...     5.33 

Silica 7.03 

Alumina 2 . 21 

Iron  sesquioxide 83 

Iron  protoxide 39 

Water  .61 


100.42        99.87      100.62 


The  following  list  of  fossils  includes  all  that  I  have  observed  in 
the  Trenton  beds.  The  determinations  are  mostly  by  Mr.  E.  P.  Whit- 
field: 

Name.  Horizon  at  which  found. 

Petrctia  (Streptelasma)  corniculum,        -  Occurs  throughout  the 

Buff  but  most  com- 
mon in  the  lower  part. 

Columnaria  alveolata,         .......  Lower  part  of  Buff. 

Graptolitic  markings,      ------  Lower  part  of  Blue. 

Crinoidal  columns,  ......  Upper  part  of  Buff. 

Otihis  tricenaria,    -------  Buff. 

Streptorhynchus  filitextus  .....  Buff. 

S.    deflectus -  Buff. 

Strophomena  camerata,      ......  Buff. 

S.    incrassata,         -        -        -        -  -  Buff. 

Rhynchonella,  n.  sp.,          ......  Buff. 

R.    n.  sp., Blue. 

Tellinomya  cuneata,   -------  Buff. 

CypricarditeS  ventricosus        -----  Buff. 

Raphistoma  lenticulare      ------  Buff. 

R.    Nasoni,  .......  Buff. 

Trochonema  umbilicatum  -----  Buff. 

Murchisonia  bicincta,     ------  Buff. 

M.    tricarinata,         -------  Buff. 

Pleurotomaria  subconica, Buff, 

Helicotoma  planulata,        ......  Buff. 

Orthoceras  annulum,      ------  Buff. 

0.    vertebrale,  .......  Buff. 

Gyroceras  duplicostatunb  n.  sp.,      -  Buff. 

Oncoceras  pandion,    -------  Buff. 

Cyrtoceras,  mid.  sp.,        -        -        -        -        -        -  Buff. 

Beside  these,  obscure  and  fragmentory  casts  of  Orthoceratites  are 
very  numerous  indeed  in  the  Buff,  varying  greatly  in  size,  some 
occurring  as  great  as  6  feet  in  length  and  8  inches  in  diameter.  The 
fossils  of  the  Buff  are  almost  wholly  in  the  state  of  casts  of  the  in- 
terior, or  impressions  of  the  exterior.  Of  those  in  the  list,  the  most 
frequently  met  with  are  the  coral  Petram,  and  the  gasteropods, 
amongst  which  Trochonema  urnbilicata  is  the  most  abundant.  These 
Wis.  SUR.--36 


502  GEOLOGY  OF  CENTRAL  WISCONSIN. 

gasteropods  are  frequently  of  very  large  size,  their  rough  casts  and 
impressions  filling  entirely  a  two-inch  layer,  whilst  for  a  number  of 
feet  above  and  below  the  rock  may  be  entirely  barren. 

The  economic  contents  of  the  Trenton  beds  are  building  stone  and 
limestone  for  flux.  Certain  beds  of  the  Blue  in  the  lead  region  are 
said  to  be  hydraulic,  and  the  property  is  probably  not  entirely  con- 
fined to  the  rock  in  that  district.  The  Trenton  limestone  is  also  one 
of  the  layers  in  which  the  lead  ore  of  the  lead  region  occurs.  A 
small  crevice  occurs  naar  the  base  of  the  Trenton,  in  the  town  of 
Fitchburg,  Dane  county,  from  which  a  few  hundred  pounds  of  galena 
have  been  taken.  For  the  most  part,  however,  the  Trenton  is  with- 
out sign  of  mineral  wealth  until  the  limits  of  the  lead  region  are 
reached,  in  the  western  towns  of  Dane  county.  East  of  this  it  occurs 
usually  in  such  small  thickness  that  it  could  not  be  looked  to  to  yield 
any  amount  of  ore,  even  if  it  should  be  metalliferous,  of  which,  how 
ever,  there  is  no  indication. 

The  Buff  limestone  is  used  for  building  everywhere  where  it  occurs. 
It  can  be  obtained  in  quite  even  blocks  and  slabs  of  suitable  thickness 
both  for  building  and  paving,  presenting,  when  laid  in  wall,  a  uni- 
form straw  color.  The  thinner  layers  are  also  frequently  used  for 
stone  fences. 

The  application  of  the  blue  or  non-magnesian  limestone  layers  as  a 
flux  in  iron  smelting  is  certainly  worthy  of  attention.  For  most  of 
the  furnaces  in  Wisconsin  and  the  northern  peninsula  of  Michigan, 
limestone  is  brought  all  the  way  from  Kelley's  Island,  in  Lake  Erie, 
whilst  others  use  unsatisfactory  native  dolomites.  The  Kelley's 
Island  rock  contains  much  more  magnesia  (15-20  per  cent.)  than  the 
Blue  limestone,  but  is  otherwise  often  purer,  carrying  almost  no 
earthy  or  silicious  impurities.  It  is  without  doubt  this  purity  that 
makes  it  prized  for  smelting  the  hard  silicious  ores  of  Lake  Superior. 
All  of  the  silica,  however,  in  the  Blue  limestone  is  in  the  state  of  clay, 
whilst  in  freedom  from  magnesia  it  ranks  far  above  the  Kelley's  Island 
stone,  and  moreover,  as  shown  by  the  third  of  the  analyses  above  giv- 
en, it  is  at  times  free  also  from  the  earthy  impurities. 

THE  GALENA  LIMESTONE. 

This  formation  is  found  in  the  Central  Wisconsin  district  only  in  a 
few  small  cappings  in  the  tovvn  of  Christiana,  eastern  Dane  county, 
and  on  the  top  of  some  of  the  narrow  ridges  of  the  towns  of  Spring- 
dale  and  Primrose,  on  the  west  side  of  Dane  county.  Since  it  is  so 
unimportant,  and  at  the  same  time  plays  so  large  a  part  in  both  the 


THE  LOWER  SILURIAN  ROCKS.  563 

Lead  Region  and  Eastern  Wisconsin  districts,  in  the  reports  on  which 
it  will  be  found  fully  described,  it  is  not  thought  necessary  to  give  it 
any  attention  here. 

II.  Local  Details.1 
POKTAGE,  WOOD,  CLARK,  AND  JACKSON  COUNTIES. 

(ATLAS  PLATE  XV,  AREA  F.) 

The  only  one  of  the  Lower  Silurian  formations  occurring  in  these  counties  is  the 
Potsdam  sandstone,  which  forms  the  basement  rock  of  the  southern  portions  of  the 
three  first  named,  the  Archaean  rocks  rising  to  the  surface  in  their  northern  portions. 
In  Jackson  county  only  the  bed  of  Black  river  and  a  few  scattering  mounds  show  the 
Archaean  rocks. 

The  peculiar  irregularities  of  the  line  of  junction  between  the  two  formations,  the  ex- 
tension southward  along  the  stream  valleys  of  long  strips  of  the  crystalline  rocks,  the 
corresponding  northward  extension,  along  the  divides,  of  the  sandstone,  and  the  difficul- 
ties met  with  in  tracing  the  boundary,  have  been  before  alluded  to.  The  facts  upon 
which  the  junction  line  for  the  region  covered  by  the  map  of  Area  F.  of  the  Atlas  is 
based,  including  the  location  of  a  number  of  outcrops,  have  also  been  given  briefly,  and 
will  not  be  repeated  here. 

A  very  large  proportion  of  the  sandstone  area  in  these  counties  is  level,  and  is,  to  a 
considerable  extent,  occupied  by  large  marshes.  Towns  21  and  22.  ranges  7  and  8  east, 
Portage  county,  are  almost  all  included  in  one  great  marsh,  as  are  also  towns  21,  ranges 
2,  3  and  4  east,  in  Wood  county,  the  latter  marsh  extending  also  over  considerable  por- 
tions of  the  towns  to  the  northward,  and  having  a  still  greater  extent  into  Juneau  and 
Jackson  counties  on  the  south.  Underneath  these  marshes,  which,  to  a  large  extent, 
have  peat  bottoms,  sandstone  is  commonly  found  at  shallow  depths.  On  some  of  the 
dividing  ridges  again,  the  sandstone  country  becomes  considerably  elevated,  and  has 
more  or  less  a  rolling  character.  Such  is  especially  the  case  with  the  divide  between 
the  Black  and  Trempealeau  rivers  in  western  Jackson  county,  which  is  without  drift 
covering,  and  is  worn  into  the  deeply  ravined  surface  characteristic  of  driftless  regions, 
The  divide  between  Black  and  Yellow  rivers,  in  western  Wood  and  eastern  Clark  coun- 
ties, is  considerably  elevated  above  the  surrounding  country,  but  is  very  heavily  coated 
with  glacial  materials,  and  presents  therefore  a  much  more  even  surface. 

The  larger  part  of  the  sandstone  area  of  Portage,  Wood,  Clark,  and  eastern  Jackson 
counties,  is  within  the  region  of  heavy  timber,  chiefly  pine.  In  the  southern  portions  of 
the  three  first  named,  and  in  a  large  part  of  western  Jackson,  small  pines  mingle  with 
the  small  oaks  tha*~.  are  characteristic  of  nearly  all  of  Central  Wisconsin,  the  growth  of 
timber  in  all  of  these  portions  being  scant  and  small,  and  associated  with  a  loose,  sandy 
soil.  On  the  northern  part  of  the  divide  between  Yellow  and  Black  rivers,  however, 
the  sandstone  is  deeply  buried  beneath  clay  drift,  as  a  result  of  which  we  find  excellent 
clay  soils,  and  a  heavy  growth  of  hard  wood  timber,  for  the  most  part  maple. 

Usually  the  sandstone  of  these  counties  is  but  a  thin  covering  upon  the  crystalline 
rocks,  which  appear  in  all  of  the  deeper  stream- valleys.  High  bluffs  of  the  sandstone, 

i  In  the  manuscript,  this  division  of  the  report  includes  a  full  description,  by  townships,  of  a 
large  part  of  the  country  occupied  by  the  Lower  Silurian  formations,  embracing  topography,  sur- 
face features,  rock  outcrops,  etc.  It  has  been  found  necessary,  in  order  not  to  erzcaed  the  limits 
originally  assigned  to  this  report,  to  throw  out  most  of  this  material,  and  a  number  of  important 
outcrops  are  therefore  not  alluded  to.  This  omission  can  be,  in  part,  made  up  for,  by  any  one  who 
wishes  further  information  than  given,  by  a  study  of  the  Atlas  maps  in  connection  with,  the  lists  of 
altitudes  of  Chapter  I.  The  whole  amount  of  material  thrown  out  would  make  ahont  45  pages  of 
the  small  typo.  K.  D.  I. 


56-i  GEOLOGY  OF  CENTRAL  WISCONSIN. 

however,  occur,  carrying  its  thickness  up  into  the  hundreds  of  feet,  and  bearing  witness 
to  the  great  thickness  which  once  must  have  existed  over  all  the  region. 

In  Sec.  23,  T.  21,  R.  8  E.,  Portage  county,  on  the  edge  of  the  great  Plover  marsh, 
rises  a  prominent  knob  of  sandstone,  known  as  Mosquito  Mountain.  The  bluff'  is  about 
100  feet  high,  with  its  main  extent  east  and  west.  Just  west  of  it,  on  the  west  side  of 
the  Portage  and  Stevens  Point  road,  is  a  second  lower  knob.  Near  the  base  of  the  main 
hill,  the  sandstone,  as  seen  in  a  quarry  (789),  is  rather  line-grained  and  light-colored,  with 
brownish  spots  and  laminae,  and  very  friable  indeed.  It  is  composed  of  grains  of  limpid 
quartz,  that  are  all  somewhat  rolled,  but  are  still  subangular  in  shape,  and  has  a  very 
minute  quantity  of  a  brownish  cement.  The  bedding  here  is  very  distinct,  the  layers 
running  from.  2  inches  to  1  foot  in  thickness  on  a  quarry  face  of  15  feet.  One  hundred 
yards  to  the  east  of  the  quarry,  on  the  same  hill,  are  ledges  of  a  much  coarser  and  more  in- 
durated sandstone  (790),  which  is  in  places  almost  like  quartzite,  having  a  whitish  color, 
and  composed  of  much-rolled  grains  of  vitreous  quartz,  closely  cemented.  A  similar  rock 
(791)  occurs  in  small  exposures  up  to  the  summit  of  the  bluff.  On  the  western  bluff  a 
quarry  exposes  coarse-grained,  brownish,  moderately  firm  sandstone  (792),  having  a 
semi- vitrified  appearance  on  the  exterior. 

At  the  foot  of  Conant's  Rapids,  S.  E.  corner  Sec.  8,  T.  23,  R.  8  E.,  3D  feet  of  hor- 
izontally bedded  sandstone  show  in  the  river  bank,  overlying  gneiss.  The  lowest  layers, 
in  contact  vrith  the  gneiss,  are  hard  and  quartzite-like;  but  the  body  of  the  exposure  is 
thinly  bedded,  coarse-grained,  friable,  and  of  a  light- brownish  color. 

At  Steven's  Point,  just  below  the  railroad  bridge,  on  the  east  bank  of  the  river 
(Plate  IX,  of  Fig.  12),  thin-bedded  friable  sandstone  shows  at  the  top  of  the  bank,  the 
gneiss  being  exposed  below. 

On  the  west  side  of  the  river,  Sec.  31,  T.  24,  R.  8  E.,  is  a  low  outlier  of  sandstone, 
rising  51  feet  above  the  river.  The  sandstone  is  cut  into  deeply  at  the  south  end  of  tho 
mound,  for  the  railroad,  and  this  catting  is  expanded  into  a  quarry  at  one  point. 
Another  large  quarry  is  worked  on  the  northwest  side  of  the  hill.  In  the  cutting,  tho 
upper  layers  are  thin-bedded,  whilst  the  lower  seven  feet  is  in  heavy  layers,  and  shows 
a  light  brownish,  white,  much  indurated,  rock  (774),  of  a  medium  grain,  and  composed 
of  highly  glassy,  subangular;  quartz  grams.  Fresh  surfaces  are  quite  uniform  in  ap- 
pearance; weathered  surfaces  much  iron-stained.  Strong  joints  occur  trending  N.  15° 
W.  and  N  50°  E.  Pieces  4  by  4  by  4  %  feet  can  be  obtained  easily,  also  thin  slabs  fit 
for  flagging,  The  quarry  on  the  west  side  of  the  hill  shows  a  similar  stone,  taken  from 
higher  layers.  The  topmost  layer  in  the  quarry  is  very  beautifully  ripple-marked.  The 
stone  from  these  quarries  is  a  valuable  one,  and  is  much  used  in  building  at  Stevens  Point. 

About  four  miles  north  of  Grand  Rapids,  in  the  town  of  Rudolph,  S.  E.  qr.  Sec.  20,  T. 
23,  R.  6  E.,  Wood  county,  a  large  and  excellent  sandstone  quarry  has  been  opened  near 
the  summit  of  the  ridge,  whose  slope  for  half  a  mile  southward  shows  sandstone  ledges. 
The  quarry  face  is  20'  feet,  and  shows  very  plainly  bedded  layers  1  inch  to  2  feet  in 
thickness.  These  are  traversed  by  very  strong  joints,  trending  N.  10°  W.  and  N.  70° 
to  80°  E.  Some  of  the  joints  are  inclined,  especially  the  former  set,  most  of  which  dip  67° 
W.,  and  others  are  vertical.  Ah1  the  stone  is  tolerably  firm,  but  most  of  it  is  not  unusually 
indurated,  crumbling  easily  in  the  fingers.  Certain  layers,  however,  are  very  highly  in- 
durated, and  are  susceptible  of  quite  a  high  jpolish.  These  are  both  plain  white  and 
white  heavily  streaked  with  dark  red,  are  of  a  rather  fine  grain,  and  consist  of  sub- 
angular  grains  of  highly  vitreous  quartz.  Large  blocks  can  be  obtained,  as  also  thin 
flags  10  by  18  feet.  The  stone  is  much  used  at  Grand  Rapids,  and  has  a  considerable 
value. 

Along  the  Wisconsin  river,  from  Grand  Rapids  to  Point  Bass,  sandstone  is  fre- 
quently exposed.  Several  sections  in  the  vicinity  of  Grand  Rapids,  showing  sandstone 
overlying  kaolin,  have  already  been  described. 


THE  LOWER  SILURIAN  ROCKS.  565 

Near  Point  Bass,  on  both  sides  of  the  river,  heavy  ledges  of  sandstone  overlie  gneiss 
(see  Figs.  2,  3  and  4).  On  the  east  side  of  the  river  the  sandstone  cliff  is  30  to  40  feet 
high.  On  the  west  side,  near  the  north  line  of  Sec.  15,  on  a  side  channel  of  the  river, 
dry  at  the  time  of  our  examination,  5  feet  of  very  friable,  coarse,  brownish  sandstone 
shows  in  the  bank,  the  upper  layer  heavy,  the  lower  ones  thinner.  The  bottom  of  the 
channel  is  formed  of  large  flat  slabs  of  the  same  sandstone,  one  inch  thick.  Beneath  four 
one  inch  layers  of  this  sandstone  are  two  inches  of  sandstone  highly  charged  with  the 
greenish-tinged  iron  sulphide,  marcasite,  which  in  places  almost  entirely  excludes  the 
sand.  Specimens  taken  oat  decompose  to  the  sulphate  very  rapidly.  Immediately  be- 
low, and  in  contact  with,  the  pyr  tous  layer,  is  the  Archaean  gneiss,  much  decomposed, 
but  retaining  still  its  firmness  and  bedding. 

Three-quarters  of  a  mile  east  of  Mapleworks,  on  the  S.  E.  qr.  of  Sec.  12,  T.  24,  R. 
1  E.,  Clark  county,  is  an  isolated  sandstone  bluff  100  feet  high,  500  yards  in  diameter  at 
the  base,  100  yards  long  and  10  wide  at  top,  rising  above  the  general  level  of  the  divide. 
The  slopes  are  covered  with  clay  and  fragments  of  sandstone.  At  the  summit  5  feet  of 
very  coarse  grained,  rather  firm,  brownish  sandstone  (982)  is  exposed,  consisting  of  very 
much  rolled  grains  of  dull  white  quartz.  The  layers  are  6  to  18  inches  in  thickness. 

About  one  mile  north  of  Neillsville,  on  the  S.  W.  qr  of  Sec.  11,  T.  24,  R.  2  W.,  10 
feet  of  cross-laminated,  coarse-grained,  yellowish  sandstone,  shows  alongside  of  the 
road.  Clay  seams,  one  to  two  inches  thick,  are  included  between  the  layers  of  sand- 
stone. Similar  sandstone  is  seen  at  the  crossing  of  Black  River,  one  mile  west  of  Neills- 
ville,  S.  W.  qr  of  Sec.  15,  T.  24,  R.  2  W.  The  base  of  the  sandstone  is  40  feet  above 
the  river;  below  is  a  slope  10  feet  in  height,  without  exposure,  and  below  this,  again, 
30  feet  of  light-colored  pinkish  granite. 

Along  Black  River,  from  Neillsville  to  Black  River  Falls,  T.  21,  R.  4  W.,  Jackson 
county,  sandstone  is  quite  frequently  exposed  in  or  near  the  banks  of  the  river,  the  bed 
of  which  is  on  the  crystalline  rocks. 

On  the  S.  W.  qr  of  Sec.  3,  T.  24.  R.  2  W.,  west  of  the  river,  is  a  sandstone  outlier  175 
feet  high,  and  about  one-third  of  a  mile  in  length,  the  upper  portions  of  which  are  per- 
pendicular ledges  of  bare  rock.  The  sandstone  is  heavily  bedded,  indurated,  coarse- 
grained, and  light-colored.  From  the  summit  of  the  bluff  a  number  of  other  similar 
outliers  can  be  seen,  dotting  the  country  to  the  west  and  south,  and  one  or  two  to  the 
north,  in  T.  26,  R.  2  W. 

For  half  a  mile  below  French's  mill,  Sec.  25,  T.  23,  R.  3  W.,  the  Neillsville  road  fol- 
lows the  west  bank  of  the  river,  at  an  elevation  of  about  30  feet  above  the  water.  On 
the  east  side  of  the  road,  granite  is  exposed  in  the  river  bank,  and  on  the  west  side  a 
ridge  of  horizontal  sandstone,  30  to  50  feet  high.  The  sandstone  is  cross-laminated, 
coarse,  yellowish,  and  made  up  of  much  rolled  quartz  grains,  which  reach  sometimes  as 
much  as  one-eighth  of  an  inch  in  diameter. 

In  T.  21,  R.  4  W.,  and  T.  22,  R.  4  W.,  ledges  of  sandstone  form  the  river  bank  for 
long  distances,  rising  20  to  40  feet  from  the  water,  and  are  in  a  number  of  places  to  bs 
seen  overlying,  or  abutting  against,  Archa?au  schists,  as  heretofore  described  (see  Plate 
XVII,  and  Figs.  1,  2Q  and  21).  This  sandstone  is  usually  of  light  yellowish  color, 
coarse,  and  somewhat  indurated,  and  includes  beds  of  red  and  green  sandy  shale.  The 
lowest  layers  are  often  affected  by  a  very  marked  cross-lamination,  the  thickness  s6  af- 
fected being  often  as  much  as  six  to  ten  feet. 

At  Black  River  Falls,  sections  15  and  22,  T.  21.  R.  4  W.,  the  crystalline  rocks  are 
largely  exposed,  the  river  passing  through  a  gorge  in  the  gneiss  and  granite.  The 
ground  rises  rapidly  from  the  river  on  both  sides,  especially  the  western,  and  on  both 
sides  the  granite  and  gneiss  are  overlaid  by  sandstone.  At  the  top  of  the  lull  on  which 
the  High  School  building  stands,  wells  pass  through  80  feet  of  sand  and  gravel  into  sand- 
stone. 


566  GEOLOGY  OF  CENTRAL  WISCONSIN. 

Opposite  Leonard's  old  mill  (Fig.  20),  in  the  bend  of  the  river  below  the  village,  25 
feet  of  sandstone  overlie  the  gneiss.  The  sandstone  here  is  the  usual  coarse  crumbly 
rock,  and  includes  layers  of  greenish  and  reddish  shale,  the  lowest  layer  being  a  fino 
conglomerate,  8  inches  in  thickness. 

Near  the  railway  depot,  on  the  west  side  of  the  river,  is  a  quarry  in  the  sandstone 
layers  belonging  just  above  those  exposed  at  the  mill.  The  quarry  face  is  15  feet  high, 
and  traversed  by  strong  vertical  joints.  The  stone  (1012)  is  heavily  bedded,  much  in- 
durated, of  a  light  color,  and  composed  of  alternating  very  coarse  and  finer  grained 
layers,  ah1  being  composed  of  rolled  grains  of  glassy  quartz.  Some  of  the  layers  show 
cross -lamination.  This  stone  is  a  valuable  one,  and  resembles  that  from  the  quarries 
already  alluded  to  as  occurring  near  Grand  Rapids  and  Stevens  Point. 

About  a  mile  southeast  of  the'  depot,  on  Sec.  23,  is  a  very  bold  sandstone  outlier  rising 
about  250  feet  above  its  base.  In  the  lower  slopes  the  sandstone  is  mostly  concealed. 
Above  is  a  perpendicular-faced,  jagged  crest,  over  100  feet  in  height,  the  prevailing 
rock  (1013)  on  which  is  a  white  to  buff-colored,  fine-grained,  firm  sandstone,  composed 
of  sub-angular  to  rounded  quartz-grains,  and  containing  near  the  top  numerous  iron- 
stained  impressions  of  Obolella  polita,  but  no  shells. 

About  one  mile  west  of  Black  River  Falls,  on  the  road  westward  to  the  Trempealeau 
valley,  is  an  exposure  of  thin-bedded,  coarse,  brownish,  crumbling  sandstone  (1010), 
with  numerous  white  fragments  of  shells  of  Obolella  polita,  which,  in  some  of  the  layers, 
make  up  most  of  the  rock.  Thin  clayey  layers  occur  in  which  a  few  shells  were  noticed, 
one  of  Lingulepis  pinnceformis.  The  outcrop  appears  to  be  130  to  150  feet  below  the 
Obolella  sandstone  of  the  bluff  near  the  depot. 

In  the  various  exposures  in  the  vicinity  of  Black  River  Falls,  we  have  a  total  thickness 
of  sandstone  of  about  350  feet,  with  two  fossil  horizons  .made  out,  one  200,  the  other  300 
feet,  above  the  gneiss  base  upon  which  the  pile  rests,  and  both  showing  Obolella  polita. 

On  the  west  side  of  the  Trempealeau  valley,  Sec.  2,  T.  22,  R.  5  W.,  Jackson  county, 
is  a  peculiar  isolated  bluff  known  as  the  Silver  Bluff.  At  the  east  end  the  bluff  is 
]  65  feet  high,  the  lower  slopes  being  covered  with  a  talus  from  the  ledges  above.  Near 
the  summit  is  exposed  a  horizontally  and  very  plainly  bedded,  hard,  white  quartzite  (1011 ), 
which  rings  like  steel  when  struck  with  the  hammer.  The  layers  are  alternately  thin 
and  thick,  and  brownish- weathered,  and  include  interstratified  layers  of  friable  sand- 
stone. The  quartzite  shows  distinctly  lines  of  lamination,  and  has  a  very  plain  granular 
texture,  being  composed  of  grains  of  vitreous  quartz  which  appear  as  if  fused  together, 
and  is  quite  highly  translucent.  It  is  unlike  the  quartzite  of  the  Baraboo  ranges,  or 
that  of  the  hills  near  Wausau,  Marathon  county.  It  contains  very  abundant  fragments 
of  casts,  more  rarely  perfect  casts,  of  a  very  large  conical  fossil  which  Mr.  Whitfield  de- 
termines as  a  new  species  of  Palceacmcea.  Following  the  bluff  along  the  brow  of  its 
southwest  face,  the  quartzite  layers  are  seen  to  continue  for  about  a  third  of  a  mile, 
when  a  sudden  rise  in  the  bluff  of  80  feet  exposes  thin-bedded,  firm,  dark  reddish- 
brown,  highly  ferruginous,  sandstone  (1016),  of  a  medium  grain,  and  composed  of 
rounded  grains  of  glassy  quartz,  which  are  stained  both  externally  and  internally  by 
iron-oxide.  On  the  north  flank  of  the  hill,  at  the  same  elevation,  as  the  quartzite  on  the 
opposite  side,  an  8  inch  layer  of  hard,  white  quartzite  is  seen,  between  heavy  beds  of 
whitish  friable  sandstone. 

JUNEATJ   AND   ADAMS    COUNTIES. 
(ATLAS  PLATES  XIV  AND  XVIII,  AREAS  E.  AND  H.) 

These  two  counties  constitute  a  rectangular-shaped  district,  lying  in  the  very  heart  of 
the  state,  about  42  miles  from  north  to  south,  by  36  from  east  to  west,  and  having  an 
area  of  about  1,475  square  miles.  Throughout  the  whole  area,  except  on  the  small 


THE  LOWER  SILURIAN  ROCKS.  567 

quartzite  bluffs  at  Necedah,  and  in  one  or  two  very  small  and  somewhat  doubtful  eap- 
pings  of  limestone  in  the  southwestern  towns  of  Juneau  county,  the  Lower  sandstone  is 
the  surface  rock. 

i  The  larger  portion  of  the  district  presents  the  character  of  a  level  plain,  which  has, 
for  the  most  part,  a  surface  of  loose  sand  derived  directly  from  the  disintegration  of  the 
Lower  sandstone,  but  showing  many  marshes,  some  of  very  large  size,  and  occasionally 
prairies.  Except  on  the  marshes,  and  the  few  small  prairies,  this  plain  is  nearly  every- 
where covered  with  a  growth  of  stunted  oaks,  with  which,  towards  the  north,  small 
"jack- pines  "  intermingle.  It  is  traversed  centrally  from  north  to  south  by  the  Wiscon- 
sin river,  and  is  surrounded  on  all  sides  by  higher  ground.  The  elevation  on  the  north 
is  due  merely  to  the  gradual  rise  of  the  plain  in  that  direction,  the  general  altitude  on 
the  southern  edge,  along  the  Lemonweir  river,  being  about  300  feet,  that  along  the  north 
line  of  Juneau  county,  400  feet.  The  high  ground  on  the  east  is  also  due  to  a  steady, 
but  very  much  more  rapid,  rise  of  the  plain  in  that  direction,  the  dividing  ridge  along 
the  line  of  Adams  and  Waushara  counties  having  an  altitude  of  some  200  feet  above 
the  Wisconsin.  On  the  south,  southwest  and  west,  however,  the  edge  of  the  plain  is 
very  sharply  defined  by  a  narrow  and  much  indented  dividing  ridge,  which  is  especially 
marked  in  the  southwestern  towns  of  Juneau  county,  where  it  has  on  its  western  side 
the  deeply  carved  valley  of  the  Baraboo,  with  its  numerous  branch  ravines. 

Dotting  the  central  plain,  and  rising  quite  abruptly  from  its  most  level  portions,  are 
the  isolated  mounds  and  castellated  peaks  of  rock  that  constitute  its  most  marked  and 
peculiar  characteristic.  Except  the  quartzite  mound  at  Necedah,  these  are  altogether 
of  sandstone,  being  the  only  portions  that  have  been  left  from  the  denudation  of  the 
Lower  sandstone.  Although  none  of  them  exceed  300  feet  in  height,  and  but  few  200 
feet,  they  register  a  denudation  of  fully  500  feet;  that  is  to  say,  over  the  larger  part  of 
this  plain  there  has  been  at  one  time  a  thickness  of  500  feet  of  rock,  wluch  no  longer 
exists,  and  possibly  there  has  been  a  much  greater  thickness  than  this.  There  are  two 

FIG.  35. 


OUTLINES  OP  ROCHE  A  Cms  AND  FRIENDSHIP  MOUND,  AS. SEEN  FROM  PILOT  KNOB. 
Seale  2.480  feet  to  the  inch. 

classes  of  these  remarkable  outliers :  the  larger  and  more  prominent  ones,  which  reach 
elevations  of  from  150  to  300  feet,  have  lengths  of  from  ^  to  1  mile,  and  show  more  or 
less  vegetation  on  top;  and  the  smaller  and  less  conspicuous  ones,  which  are  from  30  to 
100  feet  in  height,  often  of  bare  rock,  and  cover  comparatively  small  areas.  The  larger 
outliers  are  few  in  number,  and  are,  for  the  most  part,  quite  distant  from  one  another. 
Two  of  these  are  especially  prominent,  showing  from  any  point  on  or  around  the  plain 
high  enough  to  be  above  the  tree  tops.  These  are  the  Roche  a  Oris  and  the  Friend- 
sliip  Mound  in  the  southwest  part  of  T.  18,  R.  6  E.,  Adams  county.  Their  prominence 
is  due  both  to  their  heights  above  the  plain  at  their  bases  and  to  the  comparatively 
great  elevation  of  the  portion  of  the  plain  on  which  they  stand.  The  Roche  a  Cris  is  a 
thin,  wedge-shaped  mass  of  rock,  without  pinnacles,  having  a  length  of  about  £  mile, 
and  a  height  of  225  feet  above  its  base,  or  about  660  feet  above  Lake  Michigan,  and 
standing  up  like  a  fragment  of  a  great  wall.  Friendship  Mound  is  about  half  a  mile 
south  from  Roche  &  Cris,  which  it  exceeds  in  height  by  50  feet,  having  also  a  much 
greater  length  and  thickness  and  a  more  rounded  contour.  The  outline  of  these  two 
bluffs,  aa  sketched  from  the  summit  of  Pilot  Knob,  10  miles  east,  is  given  in  Fig.  35. 
Amongst  the  other  large  outliers  may  be  mentioned  the  very  large  wooded  mound,  in  T. 


568  GEOLOGY  OF  CENTRAL  WISCONSIN. 

20,  R.  6  E.,  13  miles  north  of  Roche  a  Cris;  Petenwell  Peak,  a  very  narrow  bluff  230 
feet  high,  and  with  serrated  crest,  on  the  west  shore  of  the  Wisconsin,  Sec.  9,  T.  18,  R. 
4  E.;  the  group  of  bluffs  6  to  8  miles  south  of  Friendship;  the  large  wooded  bluft'6 
miles  southeast  of  Mauston,  T.  15,  R.  4  E.;  and  the  Elephant's  Back,  near  Kilbourn 
City.  The  last  two,  though  high,  do  not  stand  out  very  prominently,  as  seen  from 
points  within  the  plain,  on  account  of  their  nearness  to  the  high  ground  that  limits  it  on 
the  south.  The  quartzite  bluff  at  Necedah  is  also  quite  prominent.  Of  the  smaller 
sandstone  outliers  there  are  a  great  number  and  variety.  Many  of  them  are  simple 
peaks  or  towers  of  rock,  having  a  diameter  at  base  of  only  a  few  feet,  and  40  to  60  feet 
in  height,  in  some  cases  the  diameter  at  base  being  less  than  that  at  the  summit.  Oth- 
ers are  a  series  of  pinnacles  or  rounded  towers  joined  together,  and  others  again  are 
massive  bluffs  with  wooded  summits  and  perpendicular  sides  of  rock. 

The  high  ground  that  bounds  the  plain  on  the  west  enters  Juneau  county  on  the  west 
side  of  T.  16,  R.  2  E.  (Fountain),  carrying  on  the  county  line  a  capping  of  the  Lower 
Magnesian  limestone.  From  here  it  trends  southeastward  across  the  towns  of  Foun- 
tain, Plymouth,  Lindina,  Wonewoc  and  Summit,  reaching  elevations  of  500  to  600  feet, 
and  then,  veering  more  to  the  eastward,  across  the  towns  of  Seven  Mile  Creek  and  Lyn- 
don to  the  Wisconsin  river,  where  it  is  cut  through  by  that  stream  in  the  gorge  known 
as  the  Dalles  of  the  Wisconsin.  This  ridge  is  very  well  marked  on  its  northern  side, 
rising  abruptly  from  the  plain,  towards  which  it  presents  a  face  deeply  indented  by  the 
streams  flowing  northward  from  it,  and  flanked  by  isolated  outliers  of  sandstone.  Until 
it  nears  the  Wisconsin,  it  constitutes  the  divide  between  the  waters  of  the  Baraboo 
and  Lemonweir  rivers.  The  former  of  these  streams  enters  Juneau  county  on  the  west 
line  of  the  town  of  Plymouth,  through  which,  as  also  through  the  next  town  on  the 
south,  it  passes  in  a  nearly  southerly  direction  to  the  south  line  of  the  county,  having  all 
along  a  narrow  rock- walled  valley,  into  which  tributary  streams  come  through  deep 
ravines,  that  set  back  into  the  higher  ground  on  each  side.  Thus  throughout  all  of  these 
southwestern  towns  of  Juneau,  the  country  bears  quite  a  different  aspect  from  that  of 
other  portions  of  the  county,  being,  in  general,  an  elevated  region,  carved  into  numer- 
ous ravines,  and  presenting,  on  the  higher  portions,  a  very  excellent  clay  soil,  although 
entirely  without  the  drift  area.  As  the  Dalles  are  approached,  the  ridge  lessens  in 
elevation,  and  shows  on  its  northern  side  many  sandstone  escarpments,  which  are  often 
worn  into  fantastic  ."hapes.  East  of  the  Wisconsin,  the  encircling  high  ground 
continues,  curving  rapidly  to  the  northeast  and  north,  through  the  towns  of  Dell  Prairie 
Sprmgville,  Jacks6n  and  New  Chester,  running  thence  northward  along  the  east  line 
of  Adams  county,  and  reaching  elevations  of  200  to  300  feet  above  the  Wisconsin  river. 
Its  character,  however,  is  now  quite  changed,  the  slopes  being  no  longer  abrupt  nor 
worn  into  ravines,  whilst  the  whole  surface  is  heavily  drift-covered. 

The  plain,  thus  encircled  by  high  ground,  would,  over  the  greater  part  of  its  area,  be- 
come covered  by  water,  if  the  gorge  at  the  Dalles  were  closed.  That  such  may  actually 
have  been  the  case  at  some  time,  is  indicated  by  the  general  appearance  of  the  plain  and 
its  surroundings,  bj  its  numerous  large  marshes,  by  the  finely  laminated  (lacustrine?) 
clay  deposits  that  occur  in  places  over  it,  and  by  the  great  bank  of  rolled  pebbles  and 
bowlders  of  quartzite  that  flanks  the  quartzite  bluff  at  Necedah,  far  within  the  driftless 
region. 

In  the  valley  of  the  Upper  Baraboo,  and  on  the  adjoining  high  ground,  in  the 
t)wns  of  Fountain,  New  Lisbon,  Plymouth,  Lindina,  Wonewoc  and  Summit,  Juneau 
county,  the  sandstone  is  frequently  exposed.  The  immediate  valley  of  the  river  is  nar- 
row, and  frequently  bounded  by  rock  walls,  20  to  120  feet  in  height,  which  show  gen- 
erally rather  friable,  medium-grained,  brownish  to  white,  sandstone,  without  trace  of 
calcareous  or  dolomitic  ingredients.  In  places,  as  on  the  east  side  of  the  river  at  Elroj-, 
near  the  railroad  bridge,  firm  quarry  layers  occur.  The  high  ground  on  either  side  of. 


THE  LOWER  SILURIAN  ROCKS.  569 

the  valley  rises  rapidly  from  it,  200  to  300  feet,  but  shows  sandstone  only,  except  in  one  or 
two  places  where  exceptional  elevations  are  reached.  One  such  place  is  on  the  county  line 
in  the  southwest  corner  of  the  town  of  Wonewoc,  just  south  of  which,  on  the  S.  E.  qr.  of 
the  N.  E.  qr.  of  Sec.  6,  T.  13,  R.  2  E.,  Sauk  county,  the  Lower  Magnesian  limestone  is 
quarried,  at  an  elevation  of  300  feet  above  the  railroad  track  at  the  village  of  Wone- 
woc, or  at  a  total  altitude  of  630  feet.  Only  a  small  thickness  (3  to  4  feet)  of  limestone 
is  exposed,  and  immediately  below  are  seen  ledges  of  coarse,  brownish,  non-calcareous1 
sandstone,  intermingled  with  which,  and  in  the  uppermost  layers  predominating,  is  a 
whitish,  chert-like  material,  having  somewhat  the  appearance  of  a  grayish,  granular 
quartzite  (1350).  Limestone  appears  also  to  cap  the  high  ground  in  Sec.  1  of  Wonewoc, 
and  in  portions  of  the  corner  sections  of  the  three  adjoining  towns.  The  limestone  was 
not  seen  here  in  place,  but  on  the  north  side  of  the  ridge  large,  fallen  m-asses  were  noticed, 
showing  the  ordinary  characters  of  the  Lower  Magnesian;  and  the  sandstone  exposures 
do  not  extend  to  the  summit.  On  the  west  side  of  the  ridge,  where  the  Mauston  and 
Wonewoc  road  descends  into  the  valley  of  a  small  stream  on  the  north  side  of  Sec.  12, 
50  feet  of  red  and  pink,  friable,  finely  laminated,  non-calcareous  sandstone,  with  firm, 
white  bands  (1340)  are  exposed.  The  white  bands  are  exceedingly  fine-grained,  and 
made  up  of  sharply  angular  grains  of  glassy  quartz,  being  in  this  respect  quite  different 
from  most  of  the  sandstone  of  the  Potsdam  series.  Scolithus  occurs  quite  abundantly 
in  this  rock.  On  tho  south  side  of  the  stream,  sandstone  is  again  exposed  of  similar 
character,  and  rising  higher,  the  uppermost  layers  containing  the  peculiar  quartzitic  or 
cherty  material  (1353)  mentioned  above  as  occurring  just  beneath  the  limestone  on  Sec. 
6,  T.  13,  R.  2  E.  The  highest  point  of  this  sandstone  is  about  15  to  20  feet  below  the 
summit  of  the  ridge  in  Sec.  1. 

From  the  lowest  exposures  along  the  Baraboo  river  to  the  limestone  on  the  tops  of  tho 
ridges,  the  whole  thickness  of  sandstone  is  not  less  than  300  feet.  The  peculiar  red- 
and- white-banded  and  cherty  sandstone  occurring  just  beneath  the  limestone  appeal's 
to  be  without  doubt  in  the  Madison  horizon,  but  with  an  unusual  thickness.  The  Men- 
dota  limestone  was  not  noticed  anywhere  in  the  region,  though  benches  occur  on  tho 
hills,  at  the  proper  elevation,  which  might  be  due  to  its  presence.  The  dolomitic  bands 
that  characterize  the  Upper  Potsdam  further  southward,  were  also  not  seen. 

Along  the  northern  face  of  the  watershed  between  the  Earaboo  and  Leinonweir  rivera, 
from  Camp  Douglas  to  the  Dalles,  numerous  isolated  bluffs  and  towers  of  sandstone  oc- 
cur. At  Camp  Douglas  Junction,  Sec.  28,  T.  17,  R.  2  E.,  is  a  group  of  -these  bluffs, 
and  a  number  more  occur  within  a  radius  of  two  or  three  miles.  Target  Bluff,  a  few 
rods  west  of  the  depot,  is  a  flat-topped  mass  of  sandstone  about  %  of  a  mile  long,  and 
120  feet  high,  with  nearly  vertical  sides.  The  lowest  layers  are  thick,  cross-laminated, 
coarse,  non-calcareous,  brownish,  and  exceedingly  friable,  having  almost  no  coherence. 
The  same  characters,  except  the  cross  lamination,  are  persistent  nearly  to  the  top,  where 
thin,  lighter- colored,  medium-grained  layers  (1353)^)  are  seen,  made  up  of  much  rolled 
grains  of  dull,  translucent  quartz.  It  is  noteworthy  that  many  of  the  bluffs  in  tin's  vicin- 
ity have  the  same  elevation,  a  f  act  evidently  to  be  attributed  to  the  existence  at  that  ele- 
vation of  some  peculiar  layer  in  the  sandstone  series. 

Immediately  south  of  the  village  of  Mauston,  on  Sec.  13,  T.  15,  R.  3  E.,  is  a  large 
and  very  prominent  sandstone  bluff,  about  200  feet  high,  half  a  mile  long  in  a  north 
and  south  direction,  and  surrounded  on  all  sides  by  vertical  cliffs  flanked  below  with  a 
long  talus  of  loose  sand  and  sandstone  fragments.  The  cliffs  are  boldest  on  the  eastern 
face,  where  they  run  from  50  to  100  feet  in  height.  One  hundred  and  eighty  feet  above 
the  base  is  a  flat  bench,  above  which  a  narrow  ridge  rises  some  20  to  30  feet,  carrying 
the  summit  of  the  bluff  to  a  total  altitude  of  about  500  feet.  The  bench  is  due,  un- 
doubtedly, to  the  presence  of  a  layer  of  green  and  red  shale,  which  is  not  exposed, 
1.  'Whenever  this  adjective  is  used  without  qualification,  the  rock  has  been  directly  tested. 


570  GEOLOGY  OF  CENTRAL  WISCONSIN. 

but  has  been  readied  by  a  small  shaft  sunk  on  tiie  summit  of  the  bluff.  The  shaft  pen- 
etrates: ^1)  sandrock,  lower  layers  thin,  white  and  shaly,  25  feet;  (2)  green  and  red  shale 
2)^  feet,  and  ends  in  (3)  sandrock  again,  the  same  as  that  seen  on  the  cliffs.  The  green 
shale  appeal's  to  be  of  the  same  kind  as  that  known  at  several  horizons  in  the  Lower 
Sandstone  in  other  parts  of  the  state,  but  is  soft  and  clayey,  unusually  free  from  sili- 
cious  sand,  and  of  a  deep  green  color.1  The  red  shale  (1342)  is  soft,  slightly  sandy,  non- 
calcareous  and  of  a  brick-red  color.  This  shaly  layer  has  influenced  the  denudation  of 
other  bluffs  seen  to  the  southeast,  which  have  their  summits  at  the  same  elevation  as 
this  bench.  It  appears  probable  that  the  Camp  Douglas  bluffs  may  owe  their  con- 
stancy of  elevation  to  the  same  cause.  All  the  sandstone  on  the  cliffs  of  the  Mauston 
bluff  is  non-calcareous,  generally  moderately  coarse,  brownish,  pinkish  and  light-colored 
in  different  layers,  anJ  much  of  it  firm  enough  to  use  in  ouilding.  It  is  quarried  near 
the  south  end  of  the  bluff,  at  the  base  of  the  cliff,  where  firm,  heavy  layers  are  ob- 
tained of  a  light-colored,  medium-grained  rock  (1347);  and  also  at  the  summit  of  the 
cliff,  near  the  north  end  of  the  bluff.  At  the  latter  place,  immediately  above  the  quarry 
beds,  and  just  beneath  the  green  shale,  are  a  few  layers  of  a  porous,  very  friable  brown- 
ish sandstone,  with  numerous  iron -stained  points  and  cavities  and  indistinct  fossil  im- 
pressions, which  consists  of  subangular  grains  of  glassy  quartz.  On  the  cliff  below  the 
quarry  the  sandstone  is  penetrated  by  numerous  brownish  veins,  one-sixteenth  to  one- 
half  an  inch  in  width,  which,  on  close  examination,  are  seen  to  be  made  up  of  the 
grains  of  the  sandrock,  more  glassy  than  usual,  and  closely  cemented  by  a  small  amount 
of  hydrous  iron  oxide. 

In  the  southern  part  o£  the  town  of  Lyndon,  on  Sec.  28,  T.  14,  R.  5  E.,  a  narrow, 
ridgy  crest  rises  200  feet  above  the  general  level  of  the  watershed,  reaching  an  altitude 
of  nearly  700  feet  above  Lake  Michigan.  At  the  summit  a  white,  cherty  material  (1330) 
resembling  that  described  as  occurring  on  Sec.  12,  town  of  Wonewoc,  remains  in  place. 
It  is  peculiar  in  showing  numerous  little  rounded  holes,  that  give  to  the  mass  some  ap- 
pearance of  an  organic  structure.  Ten  feet  below  the  chert,  fine-grained,  non-calcareous, 
whitish  sandstone  (1332)  is  exposed,  made  up  of  grains  of  very  fine,  sharply  angular, 
glassy,  quartz,  and  resembling  that  seen  below  the  chert  on  Sees.  12  and  1,  town  of 
"Wonewoc.  The  horizon  is  evidently  the  same,  and  is  just  beneath  the  base  of  the  Lower 
Magnesian  limestone. 

The  gorge  known  as  the  Dalles  of  the  Wisconsin  has  been  briefly  described  on  a 
previous  page.  Along  the  walls  of  the  gorge,  which  are  from  50  to  100  feet  in  height, 
the  rock  is  quite  uniform  in  character,  being  coarse,  very  friable,  light  to  dark  brown  in 
color,  non  calcareous,  and  consisting  of  very  much  rolled  grains  of  quartz  (1443).  The 
most  remarkable  feature  of  these  exposures,  which  are  nearly  continuous  for  as  much  as 
seven  miles,  is  the  cross  lamination  which  affects  layers  as  much  as  12  feet  thick,  and  is 
abruptly  terminated  above  and  below  by  horizontally  bedded  layers.  The  transverse 
laminae  themselves  are  quite  thin,  and  easily  separable  from  one  another.  They  are  not 
plane,  but  constitute  much  warped  surfaces.  The  structure  is  quite  well  shown  in  the 
view  represented  on  Plate  1A,  which  is  taken  from  one  of  Mr.  H.  H.  Bennet's  excellent 
photographs.  Plate  I,  also  from  one  of  Mr.  Bennet's  photographs,  shows  a  peculiar 
erosion  form,  known  as  Stand  Rock,  which  occurs  well  up  on  the  north  face  of  the  high 
ground  through  which  the  Palles  are  cut,  and  far  above  the  gorge  itself.  It  illustrates 
well  the  way  in  which  much  of  the  lower  part  of  the  Potsdam  series  is  worn — thin  layers, 
somewhat  more  ferruginous  and  firm  than  the  rest,  though  still  quite  friable,  protecting 
the  softer,  scarcely  coherent  rock  below.  Half  a  mile  east  of  the  upper  end  of  the 
Dalles,  on  the  east  side  of  the  S.  E.  qr.  of  Sec.  21,  T.  14.  R.  6  E.,  the  "  Elephant's 

'This  green  shale  has  been  the  object  of  exploitation  as  a  copper  ore,  a  considerable  amount  of 
money  having  been  expended  in  sinking  shafts,  etc.  It  is  hardly  necessary  to  say  that  the  money 
is  thrown  away. 


THE  LOWER  SILURIAN  ROCKS.  571 

Back  "  bluff,  an  isolated  sandstone  outlier,  rises  from  the  general  level.  From  the  sum- 
mit of  this  bluff  to  the  water  in  the  river  a  measured  section  was  taken,  showivg  in  all 
a  thickness  of  310  feet  of  the  sandstone.  The  following  are  the  details  of  the  section, 
beginning  at  the  top  of  the  bluff: — 

Ft.    In.    Ft. 

1.  Unexposed 20     ..     .. 

2.  Fine-grained,  porous,  friable,  light-brownish  sandstone  (1431);   com- 

posed of  subangular  grains  of  glassy  quartz;  showing  numerous 
small  iron-stained  cavities,  and  larger  ones  filled  with  loose  ferrugin- 
ous sand;  fossiliferous,  containing  Scolithus,  numerous  small  indefi- 
nite trilobite  fragments,  and  the  pygidium  of  a  large  trilobite,  ap- 
parently Dicellocephalus  Minnesotensis ;  resembling  exactly  the  fossil- 
iferous rock  on  top  of  the  bluff,  and  just  below  the  greensand  layer, 
at  Mauston;  elevation  of  the  Mauston  rock,  470,  of  this  rock,  530. . .  0  6  . . 

3.  Unexposed 12      6     .. 

4.  Yellowish  sandstone  (1432),  resembling  No.  2;  in  upper  part  with  a 

vitrified  crust;  below,  very  loose;  carrying  Scolithus 2 

5.  Unexposed 15     .. 

6 .  Same  as  No.  4 3     . . 

7 .  Unexposed 5      6 

8.  Rather  coarse-grained,  dark-brownish,  friable  sandstone  (1433);  com- 

posed of  much  rolled  grains  of  dulled  quartz;  thickly  coated  on  exte- 
rior by  hydrous  iron  oxide;  containing  Scolithus,  and  numerous 
iron-stained  cavities;  irregularly  bedded 2  6 

9 .  Unexposed  to  foot  of  steep  ascent 27 

Total  height  of  steep  ascent 88 

1 0    Unexposed;  on  flat  bench  150  paces  wide 18 

11.  Heavily-bedded,   coarse- grained,  friable,   brown,    ferruginous   sand- 

rock,  at  top  of  vertical  cliff 6     .  • 

12.  Heavily-bedded,  white^and-brown-ljanded,  coarse  sandstone;  almost 

without  coherence;  having  in  places  an  exterior  hardened  crust 22     .. 

13.  Alternating  layers  of  pink,  brown  and  white  sandstone;  medium  to 

fine-grained,  saccharoidal;  thin  pink  layers  stand  out  in  knife  edges 
from  the  body  of  the  rock;  all  affected  by  a  vitrified  crust  composed 
of  glassy,  closely  adherent,  quartz  grains,  on  removing  which  the 
rock  within  falls  to  loose  sand;  the  crust  is  one-thirty-second  to  one- 
half  inch  in  thickness,  and  has  an  ill-defined  inner  edge 16  ..  .. 

Total  height  of  cliff —    44 

14.  Unexposed;  a  long  slope  one-half  mile  to  top  of  the  cliff  at  the  river 

bank  (Rood's  Glen) 75 

15.  Thin  layers,  one-eighth  to  two  inches  tluck,  of  light-colored,  brownish- 

tinted,  medium -grained,  sugary,  friable  sandstone  (1437,  1437^, 
1438);  composed  of  much  rolled  grains  of  dulled  quartz;  layers  pro- 
jecting in  shelves 14 

16 .  Heavy,  coarse-grained,  firm,  ferruginous  layer 1     . . 

17 .  Heavy,  projecting  layer,  with  under  surface  ripple-marked,  of  medium- 

grained,  light- brownish  sandstone  (1439);  grains  much  rolled 1      7     .. 

18.  Thin  layers  like  No,  17 4      5 

19.  Thin-bedded,  coarse,  sugary,  very  friable  sandstone  (1440);  in  alter- 

nate pink  and  brownish  seams;  cross-laminated;  the  transverse  lam- 
inae thin,  warped,  and  abruptly  terminated  above  and  below 6 

20.  Heavy  layers,  resembling  No.  19;  not  cross-laminated,  grains  some- 


572  GEOLOGY  OF  CENTRAL  WISCONSIN. 

times  very  coarse,  giving-  to  the  rock  an  appearance  of  being  made  Ft.   in.   Ft. 

up  of  grains  of  rice 6     . . 

21.  Alternating  thin  and  heavy  layers,  light-colored,  friable  (1441),  with 

some  dark  brown  ferruginous  layers  (1442);  all  very  coarse  and  rice-  .... 

like;  some  of  the  thin  layers  very  regular  and  persistent 54 

Total  height  of  river  cliff 85 


Top  of  Elephant's  Back  above  river 310 


None  of  the  sandstone  of  this  section  has  any  trace  of  calcareous  or  dolomitic  ingredi- 
ents. 

On  the  Wisconsin  river,  above  the  Dalles,  the  sandstone  is  very  frequently  seen,  botli 
in  low  mural  exposures  on  the  river  bank,  and  also  in  high  isolated  peaks.  Of  these, 
the  most  remarkable,  as  to  height,  is  that  known  as  Petenwell  Peak,  which  rises 
abruptly  from  the  west  margin  of  the  river,  on  Sec.  9,  T.  18,  R.  4  E.,  Juneau  county, 
The  total  height  of  the  peak  above  the  river  is  230  feet,  the  upper  50  to  75  feet  being 
a  narrow  vertical  crest,  worn  into  partly  separated  crags,  not  more  than  20  to  30  feet 
wide  on  top  and  about  300  feet  in  length.  The  rock  of  this  crest  is  a  light-colored,  fri- 
able sandstone,  with  a  hard,  vitrified  crust.  Below  there  is  a  long  talus  of  sand,  with 
exposures  of  thin  crumbly  rock  at  base.  The  country  around  is  a  level  sand  plain,  40  fett 
above  the  river. 

The  Roche  a  Cris,  on  the  N.  E.  qr.  of  the  S.  E.  qr.f  of  Sec.  30,  T.  18,  R.  6  E.,  Adams 
county,  has  already  been  mentioned  as  one  of  the  most  striking  of  the  great  sandstene 
outliers  of  the  central  plain.  It  rises  abruptly  from  the  surrounding  level  stretch  of 
sand,  a  wedge-shaped  mass  of  bare  rock,  225  feet  high,  1.300  feet  long  at  base,  and 
about  1,100  at  the  summit,  which  is  a  nearly  level  area  10  to  200  feet  in  width.  The 
greatest  length  of  the  rock  lies  in  a  nearly  due  north  and  south  line.  The  southern  end 
is  a  sheer  precipice,  over  200  feet  in  height.  On  the  west  side  there  is  a  steep  talus  of 
sand  creeping  up  in  places  to  within  80  feet  of  the  top.  On  the  east  there  is  also  quite 
a  long  talus,  but  the  cliffs  are  generally  as  much  as  150  feet  high.  At  the  north  end 
the  rock  is  somewhat  broken  down,  making  an  easy  ascent.  The  summit  is  without 
the  pinnacles  that  characterize  Petenwell  and  others  of  the  more  western  outliers,  and 
is  grassed  and  wooded  with  a  few  small  pines  and  scrub  oaks.  It  has  the  shape  and 
dimensions  indicated  in  Fig.  36,  the  measurements  being  made  to  the  edge  of  the  ver- 

Fig.  36. 


SHAPE  OP  THE  SUMMIT  OF  ROCHE  A  CRIB. 
Scale  300  feet  to  the  inch. 

tical  cliff  on  all  sides.  The  view  given  in  Plate  XIV  is  taken  from  a  photograph  by  Mr. 
H.  H.  Bennett  of  Kilbourn  City,  and  represents  quite  accurately  the  cliff  at  the  southern 
end  of  the  bluff.  From  top  to  bottom  of  this  cliff,  the  rock  is  a  friable  aggregation 
of  rolled  quartz  grains,  showing  only  slight  and  somewhat  indefinite  variations  in  the 
different  layers.  A  detailed  section  along  the  face  of  the  cliff,  beginning  above,  is 
as  follows: 


THE  LOWER  SILURIAN  ROCKS.  573 

Ft.    In. 

1.  Fine-grained,  porous,  very  friable,  light-brown- tin  ted;  composed  of  sub- 

angular  grains  of  very  glassy  quartz;  containing  numerous  small  cavities, 
stained  by  iron-oxide;  weathering  with  a  thin  vitrified  crust,  and  occa- 
sionally with  a  brown  iron- stain;  fossiliferous,  containing  numerous  frag- 
mentary impressions  of  trilobites  and  other  fossils,  the  markings  being 
merely  thin  ferruginous  films  coating  the  nearly  loose  sand;  most  of  the 
fossils  too  indefinite  and  fragmentary  to  be  determined,  two  species  of 
Conocephalites-]ik.e  trilobitesr  and  Triplesia  ?  primordialis,  being  the' 
only  ones  made  out  (1365) 1  6 

2.  Moderately  coarse-grained,  much  finer  than  the  last,  pure  white;  composed 

of  sub-angular  to  round  grains  of  limpid  quartz,  the  larger  grains  very 
much  rolled;  weathering  in  places  with  dark  brown  blotches,  and  every- 
where with  a  hard  quart zitic  crust;  for  the  most  part  a  solid  layer,  though 
lines  of  bedding  are  to  be  seen  on  weathered  surfaces;  forming  a  narrow 
crest  at  the  summit  of  the  cliff,  only  3  or  4  feet  wide  (1366) 3  4 

3.  Medium  to  coarse-grained,  moderately  firm,  brown  j    constituent  grains 

much  rolled;  in,  thin  irregular  layers  1  to  2  inches  in  thickness;  weather- 
ing with  a  thin  vitrified  crust  (1367) 1  5 

4.  Resembling  No.  2 1      4 

5.  Medium  to  fine-grained,  moderately  firm,  brown  and  reddish-brown;  grains 

glassy,  sub-angular  to  rolled;  in  the  interior  a  massive  bed,  but  weather- 
ing out  in  places  into  thin  layers  (1368) 7 

6.  Fine-grained,  friable,  yellowish- tinted;  composed  of  much  rolled  grams  of 

dulled  quartz;  containing  little  seams  and  patches  of  greensand;  irregu- 
lar shaly  layers  with  rough  surfaces  (1369) 1  6 

7.  Medium-grained,  rather  firm,  dirty  white;  grains  glassy  and  somewhat 

rolled;  one  layer,  subordinate  lamination  not  apparent  (1370) 1      6 

8.  Medium  to  fine-grained,  brown-and- white-banded;    in  very  thin  shaly 

layers  of  almost  loose  sand,  without  hard  weathering;  occasionally  run- 
ning into  firmer  material  (1371 ) 3 

9.  Medium  to  fine  grained,  white  to  yellowish,  moderately  firm  and  compact; 

in  one  heavy  uniform  mass  without  perceptible  subdivision  into  layers;  in 

places  a  thick  quartzitic  crust  (1372) 21      3 

10.  Medium  to  fine-grained,  close  textured;    white,  dirty  white,   brownish; 

grains  all  somewhat  rolled;  hardened  crust;  in  a  massive  layer  without 
distinct  subdivision;  top  of  the  layer  ripple-marked  on  a  large  scale,  the 
summits  of  the  ridges  2  inches  apart  (1373) 43 

11.  Medium-grained,  friable,  dark  reddish-brown;    grains  much  rolled  and 

stained  superficially  with  hydrated  iron-oxide;  one  layer  (1374) 2 

12.  Medium  to  fine-grained,  very  friable,  brownish  and  yellowish;  weathering 

into  narrow  ridgy  lines;  in  some  parts,  1  foot  thick,  cross-laminated;  sub- 
ordinate layers  not  very  well  defined,  but  marked  off  by  different  colors.  31  . . 

13.  Medium  to  fine-grained,  friable,  dirty  white  to  yellowish;  grains  rolled  and 

glassy;  in  places  brown- weathered;  upper  layers  thick,  lower  ones  thin 
and  weathering  out  in  ridges  (1375) 27 

14.  Very  coarse-grained,  porous,  friable;  white  with  brown- weathering 30 

15.  Medium  to  coarse-grained;  dark-brown,  reddish- brown,  red,  white,  and 

yellow,  in  irregular  bands  2  inches  to  1  foot  in  width,  some  layers  very 
ferruginous;  grains  glassy  and  much  rolled  (1378) 20 

16.  Very  friable,  cross-laminated,  yellowish  layer,  constituting  a  marked  hor- 

izon in  the  series,  as  seen  from  below 10     . . 


574  GEOLOOY  OF  CENTRAL  WISCONSIN. 

17.  Very  fine-grained  layers,  almost  loose  sand;  in  alternating  red,  white,  yel-  Ft- 
iow,  pink  and  brown  bands;  the  bands  usually  very  thin,  and  on  close 
inspection  often  divisible  into  still  thinner  different  colored  stripes 
(1:579);  near  the  top  the  following  succession  was  observed:  2  feet  white, 
streaked  below  with  pink;  1J^  feet  pink;  3  feet  white,  streaked  with 
pink;  1%  feet  pink,  cross-laminated;  5  feet  thin  pink  and  white  streaks  — 
the  lowest  portions  weathering  with  a  vitrified  crust  (1380)  .......  ....  20 


Total  height  of  section  ..........................  »  ..............  224    10 


None  of  the  sandstone  of  this  section  shows  any  sign  of  calcareous  or  dolonutic  ingre- 
dients. 

Half  a  mile  south  of  Roche  £  Cris,  across  the  valley  of  the  north  branch  of  the  Little 
Roche  a  Cris  creek,  is  the  much  larger  outlier,  known  as  Friendship  Mound,  which 
lies  in  the  east  part  of  Sec.  31,  stretching  southward  into  the  north  part  of  Sec.  6,  T.  17, 
R.  6  E.,  where  its  southern  eud  rises  abruptly  from  the  northern  side  of  the  Little  Roche 
a  Cris  creek.  The  bluff  is  over  three-fourths  of  a  mile  in  length,  trending  a  little  west  of 
north,  and  at  base  is  as  much  as  a  third  of  a  mile  in  width.  All  around,  at  an  elevation 
of  150  feet  above  the  base,  it  presents  a  marked  bench,  bounded  by  sandstone  cliffs  50 
to  100  feet  in  height,  which  are  flanked  below  by  a  long  talus  of  sand.  Above  the  fiat 
bench  rises  a  wooded  crest  with  several  rounded  summits,  the  highest  of  which  is  280 
feet  above  tha  base  of  the  bluff,  310  feet  above  the  bridge  at  Friendship,  and  about  750 
feet  above  Lake  Michigan.  The  whole  of  the  bluff'  is  wooded  with  oak  and  pine,  pre- 
senting in  this  regard  quite  a  different  appearance  from  the  Roche  a  Cris,  and  affording 
much  poorer  opportunity  for  examination  of  the  rock  beds.  Below  the  bench  the  suc- 
cession of  layers  appears  to  be  closely  like  that  on  the  Roche  a  Cris.  At  one  point  on 
the  west  side  of  the  mound,  just  below  the  edge  of  the  bench,  the  sand  rock  is  quarried. 
The  quarry  rock  is  moderately  firm,  uniformly  brown-tinted  and  compact,  with  distinct 
lamination  lines.  The  base  of  the  quarry  is  20  feet  below  the  top  of  the  bench,  and  ia 
finely  ripple-marked.  Similar  ripple-marks  occur  again  at  a  lower  level,  but  neither 
horizon  seems  to  be  the  same  as  that  at  which  similar  markings  were  observed  on  the 
Roche  &  Cris.  Above  the  bench  the  rock  is  mostly  concealed,  but  is  seen  at  40  feet  be- 
low the  summit,  where  it  is  coarse,  friable,  and  brown-colored,  and  intersected  by  Little 
veins  of  brown  iron-oxide.  Exposures  occur  again  at  60  feet  below  the  summit,  where 
the  rock  is  white,  friable  and  S'cofrYAws-bearing. 

On  the  south  bank  of  the  creek,  at  the  Friendship  bridge,  thin-bedded,  crumbling, 
brown-and-white-banded  sandstone  is  exposed  down  to  the  level  of  the  creek,  adding 
about  45  feet  to  the  Roche  &  Cris  section.  • 

Five  to  ten  miles  south  from  Friendship,  a  number  of  outliers  of  sandstone  occur. 
One  of  these,  Rattlesnake  Rock,  is  about  five  miles  south  from  Friendship,  in  the  south- 
ern part  of  the  town  of  Adams.  The  bluff  is  about  half  a  mile  in  length,  is  cut  into  two 
parts  by  a  central  depression  nearly  to  the  level  of  the  adjoining  low  ground,  and  is 
mostly  grassed  and  wooded.  On  each  side  of  the  gorge,  and  on  all  sides  of  the  bluff, 
are  considerable  exposures,  the  cliff  on  the  west  side  reaching  50  or  even  75  feet  in 
height.  A  marked  bench  is  130  feet  above  the  base.  Above  the  bench  the  bluff  rises 
90  feet,  the  summit  being  255  feet  above  the  bridge  at  Friendship,  and  655  feet  above 
Lake  Michigan.  So  far  as  observed,  the  rock  and  the  succession  of  layers  are  the  same 
as  in  the  Roche  a  Cris  section.  At  the  top  of  the  bluff,  the  rock  (1389)  is  fine-grained, 
very  friable,  whitish  sandstone,  made  up  of  glassy  quartz  grains,  and  closely  resembling 
the  fossil  rock  on  the  summit  of  Roche  a  Cris,  to  which  horizon  it  evidently  belongs,  as 
indicated  by  its  having  the  same  altitude,  and  numero  fossil  fragments,  as  well  as  by 
its  lithological  character.  The  fossils  are  chiefly  trilobite  fragments,  belonging,  so  far 
as  can  be  determined,  to  the  genus  Conocephalites,  and  Sc<?M/ms-borings.  Ten  feet 


THE  LOWER  SILURIAN  ROCKS.  575 

below  the  fossil  horizon,  the  rock  (1,390)  is  somewhat  the  same,  but  often  brownish  and 
containing  numerous  iron-stained  cavities.  It  is  traversed  also  in  every  direction  by 
films  and  veins  of  dark- brown  and  reddish  black  hematite.  Some  of  the  veins  are  as 
much  as  an  inch  in  width,  and  often  show  an  interior  cavity  or  "  vug,"  lined  with  black, 
dull  nietallic-lustred,  crystalline  plates,  which  have  a  distinct  cubical  cleavage  and  red- 
dish streak.  Amongst  the  plates  are  concretionary  balls,  chiefly  of  the  browner  oxide, 
%th  inch  in  diameter,  and  made  up  of  concentric  shells.  The  structure  of  the  crystal- 
line plates  indicates  that  the  hematite  has  resulted  from  an  oxidation  of  pyrite. 

One  mile  southwest  from  Rattlesnake  Rock  is  another  quite  remarkable  pile  of  rock, 
lying  in  the  midst  of  a  large  marsh.  The  summit  is  a  flat,  oval-shaped  area,  about  300 
by  1,500  feet  in  size,  the  greatest  length  being  in  a  N.  25°  W.  direction.  The  base  is 
about  35  feet  lower  than  that  of  Rattlesnake  Rock,  and  the  summit  is  155  feet  higher, 
or  about  555  feet  above  Lake  Michigan.  On  the  east  face  the  cliffs  are  50  to  75  feet  in 
height;  on  the  west,  over  100  feet.  At  the  northern  end  the  rock  is  exposed  for  most 
of  the  height  of  the  bluff,  being  worn  into  towers  partly  separated  from  the  main  rock. 

A  section  of  the  bluff,  taken  chiefly  on  the  east  side,  is  as  follows : 

Ft.     In. 

1.  Very  fine-grained,  non-friable  but  porous,  yellowish,  non-calcareous;  dotted 

with  fine  shining  scales  of  mica;  made  up  of  very  sharply  angular  quartz 
grains;  weathering  with  a  Light  yellowish  smooth  surface;  thin  lamina- 
tion indicated  by  fine  lines,  parallel  to  which  there  is  a  tendency  to  split- 
ting; filled  with  minute  fragmentary  fossil  impressions,  chiefly  of  trilo- 
bites;  among  these  were  determined  Ptt/cJuispis  (n.  sp.),  Conocepha- 
lites  minor,  and  Orthis  Barabuensij;  not  found  definitely  exposed,  but 
lying  in  fragments  thickly  strewn  over  the  surface  of  the  bluff,  which  is 
grassed,  the  rock  being  thus  concealed;  lying  about  100  feet  lower  than 
the  fossil  horizon  on  Rattlesnake  Rock,  and  the  same  horizon  on  Roche 
a  Cris;  not  a  mere  local  layer,  because  found  again  with  exactly  the  same 
fossil  contents,  and  peculiar  lithological  characters,  and  occupying  the 
same  position,  10  miles  eastward  on  Pilot  Knob;  not  appearing  in  the 
Roche  a  Cris  section,  where,  however,  it  might  easily  have  been  over- 
looked on  some  of  the  less  accessible  portions  of  the  cliff  (1400) . .  . .  6? 

2.  Very  coarse,  triable,  reddish  brown;  weathering  into  thin  layers 9 

3.  Very  coarse  and  friable,  white- and-brown  banded;  carrying  large  ripple- 

marks  at  top 1G     .. 

4.  Moderately  coarse,  friable;  uniformly  white  in  color,  except  on  weathered 

surfaces,  which  show  brown-stained  layers  2  inches  to  4  inches  in  thickness,    18     . . 

5.  Finer-grained,  very  friable,  pink-and-white  banded,  white  predominating 

below 14     .. 

6.  Coarse-grained,  very  friable;  whitish  with  dirty  colored  ridgy  projections, 

which  on  exposed  edges  are  viUified;  near  the  base  including  some  pink 

layers 19      6 

7.  Fine-grained,  very  friable,  brown- and- white-banded;  thin-laminated 8 

8.  Not  seen  in  detail 50 

9.  Alternating  very  coarse  and  finer  sand  layers,  all  very  friable;  alternating 

also  in  color,  being  banded  white  and  brown ;  finer  layers  cross-lamin- 
ated; coarser  ones  (1401)  very  plainly  banded,  and  containing  rolled 
grains  up  to  ^  to  T\j  inch  in  diameter;  all  showing  very  marked  surface 
vitrification,  which  in  the  coarser  parts  extends  in  much  further  than  in 
the  finer,  the  grains  being  glassy  and  closely  adherent;  seen  at  the  foot 
of  the  north  end  of  the  cliff 20 

Height  of  the  bluff 155     . . 


576  GEOLOGY  OF  CENTRAL  WISCONSIN. 

Nine  miles  east  from  Roche  a  Cris  and  Friendship  Mound,  on  the  N.  E.  qr.  of  Sec.  3, 
T.  17,  R.  7  E.,  is  the  outlier  known  as  Pilot  Knob.  This  is  a  narrow  jagged  crest,  75 
feet  long,  10  to  15  feet  wide,  and  80  feet  high,  resting  upon  a  hill  with  gentler  slopes, 
and  about  400  paces  in  diameter.  A  section  from  above  downwards  is  as  follows : 

Feet. 

1.  Medium  to  fine-grained,  brick-red  (1420,  770);  composed  of  rolled  grains  of 

quartz,  coated  externally  with  red  and  brown  iron  oxides;  containing  some 
hard  curving  seams,  %  to  ^  inch  in  thickness,  of  a  dark  brown  color,  made 
up  of  glassy  quartz  grains  cemented  by  much  brown  iron-oxide,  and  evi- 
dently of  a  concretionary  nature;  including  some  lighter  colored  brown  and 
even  white  layers,  the  latter  (1419)  porous,  friable,  medium- grained,  and 
weathering  with  a  very  hard  vitrified  crust;  containing  near  the  base  about 
a  foot  of  light  reddish,  veiy  friable,  fine-grained,  fossiliferous  rock,  con- 
taining Ptychaspis  Miniscaensis  and  other  trilobite  impressions 45 

2.  White,  friable,  non-fossiliferous  sandstone,  to  foot  of  crag 40 

3.  Unexposed,  on  gradual  slope -. 30 

4.  Fine-grained,  non-friable,  yellowish  sandstone  (1421),  consisting  of  fine  angu- 

lar quartz,  and  containing  a  few  scales  of  mica;  thin-bedded  and  marked 
by  fine  lines  of  lamination,  parallel  to  which  it  splits  with  some  readiness; 
fossiliferous,  containing  Ptychaspis,  Conocephalites  and  disks  of  crinoidal 
columns;  exactly  resembling  the  fossil  rock  at  the  summit  of  the  last  sec- 
tion given,  to  which  horizon  it  undoubtedly  belongs 1 

5.  Unexposed,  on  steep  slope , 10 

6.  White-and-brown-banded,  thin  friable  layers 20 

7.  Unexposed  to  base 20 


Height  of  Knob 166 


The  two  fossil  horizons  of  the  above  section  appear  to  be  the  same  as  reco^ized  on 
Roche  a  Cris,  and  the  bluffs  south  of  Friendship,  though  apparently  somewhat  nearer 
together.  The  base  of  Pilot  Knob  is  545  feet,  the  lower  fossil  horizon  595  feet,  the  up- 
per fossil  horizon  665  feet,  and  the  summit  705  feet  above  Lake  Michigan.  These 
figures  indicate  a  slight  rise,  about  4  feet  to  the  mile,  of  the  strata  between  Roche  a 
Cris  and  Pilot  Knob.  It  is  possible  that  this  rise  may  be  exaggerated  by  unreliable 
barometrical  observations;  there  is,  however,  certainly  no  rise  westward  between  these 
points. 

A  mile  and  a  half  southeastward  from  Pilot  Knob,  the  intervening  ground  being  low, 
on  the  N.  W.  qr.  Sec.  12,  T.  17,  R.  7  E.,  is  a  long  ridge  facing  northwestward,  with 
rock  outcrops  on  the  flanks.  The  highest  outcrop  seen  is  some  20  feet  below  the  top  of 
the  ridge,  and  about  25  feet  lower  than  the  summit  of  Pilot  Knob.  From  this  point 
downwards  for  40  feet  are  seen  layers  of  incoherent  white  sandstone,  with  intercalated 
yellowish  calcareous  bands,  2  to  6  inches  in  thickness,  and  5  to  15  feet  apart.  The 
rock  of  these  bands  (1405,  1406,  1407)  is  rough- textured,  porous  and  moderately  firm, 
but  crumbling  under  the  hammer.  It  has  the  appearance  of  being  coarsegrained,  but 
on  close  inspection  most  of  the  apparent  large  grains  are  seen  to  be  due  to  the  aggrega- 
tion of  smaller  ones,  and  the  rock  is  seen  to  consist  of  an  admixture  of  fine,  yellowish, 
angular  grains,  and  larger  ones  of  white  and  much-rolled  quartz,  with  sparsely  scattered 
greensand  grains.  On  solution  in  acid,  the  yellowish  matter  is  entirely  dissolved,  leav- 
ing a  residue  of  not  over  40  per  cent.,  which  is  made  up  entirely  of  the  white  quartz 
grams.  Cleavable  calcite  is  occasionally  to  be  seen  by  the  naked  eye,  and  from  Iho 
ready  effervescence  and  solution  in  cold  acid,  it  is  judged  that  the  rock  is  much  more 
largely  calcareous  than  dolomitic.  These  layers  are,  beyond  doubt,  those  that  are  to  Lo 
seen  in  more  southern  counties  immediately  underlying  the  Mendota  limestone,  which 


THE  LOWER  SILURIAN  ROCKS.  577 

possibly  exists  as  a  capping  on  this  hill.  From  the  figures  given,  it  will  be  seen  that 
these  layers  extend -as  much  as  60  feet  lower  than  the  summit  of  Pilot  Knob,  which, 
moreover,  is  of  an  entirely  different  kind  of  rock.  In  order  that  the  Pilot  Knob  layers 
may  pass  beneath  those  across  the  valley,  they  must  have  a  descent  of  at  least  50  feet 
to  the  mile  in  that  direction,  an  amount  of  descent  that  would  be  altogether  extraor- 
dinary in  Central  Wisconsin. 

One  mile  eastward  from  the  exposures  just  described,  on  the  N.  W.  qr.  of  Sec.  7,  T. 
17,  R.  8  E.,  Marquette  county,  is  a  large  isolated  bluff' capped  by  the  Lower  Magnesian 
limestone.  Another  similar  bluff  lies  a  mile  northeast  of  this  on  Sec.  4  of  the  same 
town.  The  first  named,  known  as  "Glover  and  Merriman's  lime  bluff."  shows  the  fol- 
lowing section : 

Feet. 

1.  Lower  Magnesian  limestone  (1409):  close-textured,  very  finely  crystalline,  yel- 

lowish-gray to  nearly  white;  holding  small  cavities  lined  with  brown- tinted 
dolomite  crystals,  and  others  lined  with  stalactitic  lime  carbonate;  in  places 
marked  with  fine  pencilings  of  the  dendritic  oxide  of  manganese;  dolomite — 
dissolving  only  in  heated  acid,  with  a  residue  of  very  fine,  white,  angular 
silica,  constituting  13.96  per  cent,  of  the  whole  —  but  containing  no  sand 
whatever;  containing  little  greenish  blotches  and  streaks;  weathering  with 
rough  surface;  occurring  in  layers  3  to  4  feet  thick,  some  of  which  are  much 
displaced 30 

2.  Unexposed 10 

3.  Madison  sandstone:  coarse,  whitish,  moderately  firm;  forming  a  prominent 

ledge  on  the  side  of  the  bluff 10 

4.  Unexposed , 40 

The  following  occurs  on  an  outlying  hill  south  of  the  main  bluff: 

5.  Mendota  limestone:  lowest  layers  only  seen;  brownish  and  yellowish 10 

6.  Unexposed 15 

7.  Potsdam  sandstone:  white,  crumbling  sandstone,  with  intercalated  yellowish, 

coarse-textured,  calcareous  layers  (773,  1408),  exactly  like  those  seen  at 

the  last  locality  described 10 

8.  Unexposed  to  base  of  bluff. 35 

Total  height  of  bluff. 160 


The  base  of  the  bluff  is  570  feet,  and  its  summit  730  feet,  above  Lake  Michigan. 
These  figures  indicate  some  descent  from  the  locality  on  Sec.  12,  T.  17,  R.  7  E.,  but  ex- 
actly how  much  is  not  ascertainable,  from  the  somewhat  indefinite  position  in  the  series 
of  the  limy  layers  at  the  former  place.  It  has  been  said  that  Friendship  Mound  and  the 
Roche  a  Cris  rise  respectively  to  altitudes  of  750  and  665  feet  above  Lake  Michigan. 
Neither,  however,  shows  any  sign  of  limestone  at  top,  or  any  indication  of  reaching 
within  100  feet  of  its  horizon.  This  might  be  explained  readily  enough  by  supposing  a 
continuation  westward  of  the  somewhat  rapid  rise  of  the  strata  that  is  indicated  in  the 
vicinity  of  the  Lime  Bluffs.  It  has  been  shown,  however,  that  the  strata  of  Pilot  Knob 
indicate  not  only  no  westward  rise,  but  even  a  slight  eastward  one. 

The  occurrence  of  two  limestone  outliers  as  much  as  25  miles  from  the  nearest  points 
of  the  area  occupied  by  the  Lower  Magnesian  is  interesting,  and  of  considerable  economic 
importance.  That  this  formation  once  extended  as  far  north  as  this  is  thus  rendered 
certain.  Having  reached  the  highest  land  in  the  region,  it  may  possibly  have  had  also 
a  still  wider  spread  northward. 
Wis.  SUR.  — 37 


578  GEOLOGY  OF  CENTRAL  WISCONSIN. 

MARQUETTE  AND  WAUSHARA  COUNTIES,  AND  GREEN  LAKE   COUNTY, 

OF  THE  Fox  RIVER. 


(ATLAS  PLATE  XIV,  AREA  E.) 

This  district  lies  chiefly  to  the  north  and  west  of  the  Fox  river,  towards  which  it  slopes 
steadily  from  the  summit  of  the  dividing  ridge  in  western  Waushara  and  southern 
Adams  counties.  It  includes  a  total  area  of  about  1,239  square  miles.  Throughout  the 
region  the  Potsdam  sandstone  seems  to  be  the  surface  formation  everywhere,  except  in 
the  few  places  where  the  crystalline  rocks  come  to  the  surface,  and  in  one  or  two  limestone- 
capped  bluffs.  The  sandstone,  however,  is  not  frequently  exposed,  being  for  the  most 
part  very  deeply  buried  beneath  the  glacial  drift,  or  Champlain  lacustrine  clays,  the 
former  occurring  in  portions  of  the  region  in  a  morainic  condition,  and  of  unusual  thick- 
ness. It  is  not  possible  to  be  certain  that  the  superficial  deposits  do  not  in  places  rest 
directly  upon  the  crystalline  rocks  without  intervening  sandstone,  but  the  known  facts 
render  such  an  hypothesis  improbable. 

This  region,  though  similar  in  its  basement  rock  and  general  sandy  soil  to  the  central 
plain  of  Adams  and  Juneau  counties,  differs  from  it  in  being  without  the  plain-like 
character,  presenting  as  it  does  a  steady  descent  from  northwest  to  southeast  of  over 
300  feet,  and  a  surface  in  general  much  roughened  by  morainic  drift.  Another  striking 
difference  is  found  in  the  absence  of  the  castellated  outliers  that  characterize  the  Adams 
and  Juneau  district.  A  few  small  ones  dot  the  summit  of  the  high  ground  in  north- 
western Marquette  county  and  the  adjoining  part  of  Waushara,  but  these  are  of 
rounded  shape,  comparatively  stout,  and  without  the  fragile  appearance  of  the  more 
western  peaks.  Further  east,  the  outliers  disappear  altogether.  The  general  south- 
eastward descent  gives  that  direction  to  the  many  tributaries  of  the  Fox,  which,  as  al- 
ready described,  are  large,  clear  and  rapid  streams,  furnishing  many  excellent  water- 
powers.  In  places  quite  large  areas  are  level,  as  for  instance  Burr  Oak  prairie,  in  west- 
ern Waushara  county,  but  these  are  but  small  portions  of  the  whole  district.  In  tho 
town  of  Mount  Morris  and  the  adjacent  country,  northeast  of  Wautoma,  Waushara 
county,  is  a  small  district  which  owes  its  irregularity  of  surface  chiefly  to  subaerial  ero- 
sion of  the  rocky  strata,  presenting  the  ordinary  phenomena  of  deep  and  narrow  val- 
leys. Southeastern  Marquette  county  includes  a  small  part  of  the  south  side  of  the 
Fox  river  basin,  in  the  towns  of  Packwaukee,  Buffalo  and  Montello.  The  character  of 
this  area  is  similar  to  that  of  the  rest  of  the  region,  the  sandstone  outcrops  being  some- 
what more  frequent,  but  the  surface  in  general  much  heaped  up  with  drift. 

The  soil  of  the  region  is  largely  sandy.  This  sand,  however,  though  originally  com- 
ing, without  doubt,  from  the  Potsdam  sandstone,  is  directly  derived  from  the  glacial 
drift,  which  has  also  contributed  much  calcareous  and  clayey  matter.  Thus  it  comes 
that,  although  based  upon  the  sandstone,  and  presenting  in  many  places  a  very  sandy  soil, 
excellent  farming  land  is  by  no  means  uncommon  in  these  counties.  In  the  eastern 
towns  of  Waushara  county,  where  the  red  Champlain  clays  make  up  the  body  of  the 
soil,  much  very  excellent  land  is  found.  Except  in  the  clay  region  of  eastern  Wausha- 
ra, where  hard  wood  (ash  and  elm)  is  plenty,  the  only  timber  is  for  the  most  part  the 
small  oak  growth  that  characterizes  most  of  Central  Wisconsin,  the  oaks  becoming 
mingled  with  pines  towards  the  north. 

From  what  has  been  said,  it  will  be  seen  that  the  exposures  of  horizontal  strata,  are 
not  frequent.  The  time  bluffs  of  the  town  of  Springfield,  in  the  northwestern  corner  of 
Marquette  county,  have  already  been  described.  On  Sec.  15,  T.  19,  R.  11  E.,  Waushara 
county,  the  high  ground  known  as  Mount  Morris  reaches  into  the  limy  layers  that 
underlie  the  Mendota  limestone.  On  top  of  the  hill,  240  feet  above  Mount  Morris  post 
office,  are  exposed  3  feet  of  thin  layers  of  coarse-grained,  yellowish,  firm  sandstone 


PLATE, 


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4 


THE  LOWER  SILURIAN  ROCKS.  579 

(1416),  alternating  with  finer-grained,  more  friable  layers  (1415).  The  coarser  rock  is 
the  most  calcareous,  consisting  of  much-rolled  grains  of  dulled  quartz,  with  30  per  cent, 
of  yellow-stained,  cleavable  calcite  (and  dolomite?)  grains,  and  dark,  smooth-surfaced 
grains  of  greensand.  The  horizon  is  probably  within  25  feet  of  the  Mendota,  and  is 
from  600  to  650  feet  above  Lake  Michigan.  On  the  N.  W.  qr.  of  Sec.  16,  260  feet  below 
the  rock  on  top  of  the  mount,  light  brownish,  very  fine-grained,  firm,  non-calcareous- 
sandstone  (1414%)  is  exposed.  With  the  exception  of  Mt.  Morris,  the  lime  bluffs  of  north- 
western Marquette  county,  and  a  few  points  in  the  town  of  Buffalo,  Marquette  county, 
the  whole  region  appears  to  be  eroded  well  down  into  the  Potsdam  series,  probably 
everywhere  as  much  as  100  feet  below  the  Mendota,  and  in  general  200  to  300  feet. 
Even  in  the  eastern  towns  of  Waushara,  just  east  of  which,  in  Winnebago  county,  the 
Lower  Magnesian  is  well  down  into  the  low  ground,  the  erosion  into  the  Potsdam  has 
been  very  considerable,  the  lacustrine  clays  reaching  a  thickness  of  over  100  feet.  At 
the  limestone  bluff  on  Sec.  7,  T.  17,  R.  8  E.,  Marquette  county,  the  base  of  the  Lower 
Magnesian  is  700  feet  above  Lake  Michigan.  Thirty-eight  miles  from  here,  in  a  N.  10° 
E.  direction,  on  Sec.  27,  T.  19,  R.  14  E.,  Winnebago  county,  the  same  horizon  is  at  an 
altitude  of  about  200  feet.  The  total  eastward  descent  thus  shown  is  500  feet,  or  about 
13  feet  to  the  mile.  This  descent  is,  however,  by  no  means  uniform,  being  very  much 
greater  in  the  eastern  half  of  the  distance,  for  the  place  of  the  base  of  the  Lower  Mag- 
nesian at  Mt.  Moms,  ad  indicated  by  barometrical  observations,  is  not  less  than  700  feet 
above  Lake  Michigan.  These  observations  were  far  from  any  known  point  of  altitude, 
but  allowing  all  chances  for  error,  the  altitude  of  the  Lower  Magnesian  base,  at  this 
place,  could  hardly  be  less  than  650  feet. 

Very  good,  hard,  white  sandrock  is  quarried  about  3  miles  from  Wautoma,  in  the 
town  of  Mount  Morris,  Waushara  county;  at  a  point  about  the  same  distance  north  of 
Montello,  Marquette  county;  and  again  near  the  village  of  Packwaukee,  in  the  latter 
county.  The  stone  from  all  resembles  somewhat  the  sandstone  from  the  Stevens  Point, 
Grand  Rapids  and  Black  River  Falls  quarries,  and  may  be  at  the  same  horizon.  The 
Packwaukee  quarry  is  opened  in  the  top  of  a  low  ridge,  on  the  edge  of  the  Fox  river 
marsh,  and  a  short  distance  from  the  shore  of  Lake  Buffalo,  N.  E.  qr.  of  Sec.  30,  T.  15, 
R.  9  E.  The  quarry  face  is  15  feet  high,  and  the  rock  very  regularly  bedded  in  layers 
from  2  inches  to  30  inches  in  thickness,  the  heavy  layers  occurring  below,  the  thin  ones 
at  top.  Strong,  smooth-faced  joints  intersect  the  layers,  trending  N.  75°  W.,  N.  35° 
W.,  N.  17°  W.,  and  N.  14°  E.  The  top  layers  are  somewhat  soft  and  brownish,  tho 
whole  quarry  face  being  much  iron-stained  by  weathering.  The  heavy  layers  below, 
however,  present  a  very  much  indurated,  nearly  white,  fine-grained  sandrock  (760), 
made  up  of  grains  of  sharply  angular,  glassy  quartz,  and  obtainable  in  very  large 
straight-edged,  smooth-faced  blocks,  which  dress  readily.  The  rock  is  a  quite  unusually 
good  building  material. 

SAUK  AND   COLUMBIA  COUNTIES. 

(ATLAS  PLATES  XIII  AND  XIV,  AREAS  D  AND  E.) 

Those  portions  of  Sauk  county  lying  west  of  the  west  line  of  R.  4  E.,  are  not  here  in- 
cluded. The  remainder  of  this  county,  and  Columbia,  constitute  a  nearly  rectangular 
area,  54  miles  from  east  to  west  and  24  from  north  to  south,  lying  just  midway  between 
Lake  Michigan  and  the  Mississippi  river.  Sauk  county,  in  its  southern  portion,  along 
the  Wisconsin,  oversteps  the  Limits  of  the  rectangle,  adding  three  entire  townships  and 
parts  of  three  others.  The  whole  area  of  the  district,  as  given  by  the  land-office  plats, 
is  1,351.5  square  miles,  including  785  square  miles  for  Columbia,  and  566.5  square 
miles  for  that  portion  of  Sauk  county  here  described,  the  whole  of  Sauk  county  having 
an  area  of  796.5  square  miles. 


580  GEOLOGY  OF  CENTRAL  WISCONSIN. 

The  main  topographical  features  of  the  district  —  the  east  and  west  ranges  of  the 
Baraboo;  the  Wisconsin  river,  which  traverses  the  area  centrally  from  north  to  south, 
making  a  great  bow  eastward  to  double  the  eastern  point  of  the  uniting  quartzite 
ranges;  the  remarkable  course  of  the  Fox  river,  which  after  flowing  southwest  directly 
towards  the  Wisconsin,  turns  abruptly  north  when  but  one  and  one-half  miles  from  it, 
the  two  rivers  traversing-  a  flat  sand  plain,  without  dividing  ridge,  and  passing  the  one 
into  the  St.  Lawrence,  the  other  to  the  Gulf  of  Mexico;  the  escarpment  of  the  Lower 
Magnesian  limestone,  which  crosses  Columbia  county  from  S.  W.  to  N.  E.,  having  its 
face  turned  westward  and  much  indented  by  the  head  waters  of  the  streams  tributary 
to  the  Wisconsin;  the  gentle  eastward  slope  of  the  country  east  of  the  escarpment,  with 
its  streams  flowing  eastward  to  the  Rock  river;  the  sandy  plain-like  character  of  the 
country  west  of  the  escarpment;  the  isolated  erosion  peaks  and  outliers  that  dot  the  sur- 
face of  this  plain  —  have  all  already  been  more  or  less  briefly  alluded  to. 

The  Lower  Magnesian  escarpment  enters  Columbia  county  on  the  southern  side  of 
the  town  of  Lodi,  projecting  in  bold  points  that  rise  250  to  300  feet  above  the  valley  of 
Spring  creek.  Thence  it  trends  northward  through  the  eastern  row  of  sections  of  that 
town,  with  the  same  character,  having  on  top  the  elevated  prairie  land  of  Arlington . 
At  the  northeastern  corner  of  Lodi,  it  turns  nearly  at  right  angles,  crossing  the  north- 
ern row  of  sections  of  Arlington  in  an  eastward  direction.  Passing  into  the  northwest 
corner  of  Leeds  it  turns  again  northward,  traversing  Lowville  from  southeast  to  north- 
west. In  this  town,  though  still  well  marked,  the  escarpment  is  much  lessened  in  bold- 
ness and  height,  because  of  the  increasing  eastward  descent  of  the  strata,  and  because 
also  it  has  in  front  a  wide  area  occupied  by  the  Madison  and  Mendota  beds,  beyond 
which  a  second  escarpment  leads  to  the  lower  level  occupied  by  the  Potsdam  sandstone. 
From  the  northeast  corner  of  Lowville  it  crosses  the  northwest  part  of  Otsego,  not  far 
from  the  village  of  Rio,  and  passing  into  Springvale  about  the  middle  of  its  south  line 
traverses  that  town  in  a  northerly  direction,  projecting  westward  in  long  points.  In 
Springvale  the  Mendota  and  Madison  escarpment  is  the  most  marked  of  the  two,  it  pre- 
senting long  narrow  and  bold  points  projecting  westward  between  the  branches  of  Duck 
creek,  which  head  in  the  towns  to  the  eastward.  The  main  branch  of  Duck  creek,  in 
the  northern  part  of  Springvale,  has  the  widest  valley,  and  has  on  each  side  the  longest 
of  the  Lower  Magnesian  points,  that  on  the  north  side  extending  all  the  way  to  the  west 
line  of  the  town.  On  this  branch  of  Duck  Creek,  also,  the  low  ground  extends  far  east- 
ward into  the  towns  of  Courtland  and  Randolph.  Across  the  town  of  Scott  the  escarp- 
ment presents  the  same  character  as  in  Springvale,  the  westward  projecting  points  re- 
ceding eastward,  however,  in  the  north  part  of  the  town,  and  having  between  them  the 
head  streams  of  the  Fox  river,  instead  of  tributaries  of  the  Wisconsin.  The  remarka- 
ble manner  in  which  the  Lower  Magnesian  escarpment  recedes  from  the  Wisconsin  after 
forming  for  so  many  miles  the  southern  boundary  of  the  valley  of  that  stream,  and  the 
bearing  of  this  upon  the  former  southern  discharge  of  the  Fox  river  system,  have  been 
previously  alluded  to. 

Immediately  south  and  east  from  the  limestone  edge,  the  country  is  on  a  level 
with  its  summit,  but  further  south  and  east  sinks  gradually  with  the  decline  of  the 
strata  in  those  directions.  Along  the  western  part  of  the  soutli  line  of  Columbia  county 
the  direction  of  the  greatest  descent  of  the  strata  is  nearly  due  south:  further  east  and 
north,  however,  it  veers  to  the  eastward,  being  at  the  middle  of  the  east  line  of  the 
county  about  due  east.  Still  further  north,  in  the  town  of  Randolph,  a  northern  de- 
scent begins  to  be  distinctly  perceptible.  The  surface  slopes  in  general  correspond 
with  these  changes  in  direction  of  the  slopes  of  the  strata.  The  greatest  elevations  are 
thus  evidently  reached  towards  the  southwest,  where  the  escarpment  is  highest.  Thus, 
the  high  prairie  of  Arlington  and  Ijeeds  reaches  altitudes  of  from  450  to  500  feet,  whilst 
tin-flier  east,  in  Columbus  and  Hampden,  the  general  elevation  is  200  to  250  feet  less. 


PLATE.  XXIil 


•n 


THE  LOWER  SILURIAN  ROCKS.  581 

Further  ideas  as  to  this  structure  can  best  be  obtained  by  examination  of  the  sections  of 
Plates  XXII  and  XXIII,  in  connection  with  the  map  of  Area  E.  In  southeastern  Lodi, 
Arlington.  Leeds,  Hampden,  southeastern  Lowville,  southwestern  Otsego,  and  southern 
Fountain  Prairie,  the  country  above  the  escarpment  is  generally  rolling  prairie,  much  of 
it  very  high.  Further  north,  in  northern  Otsego  and  Fountain  Prairie,  and  southern 
Courtland  and  Springdale,  the  prairie  belt  is  broken  by  a  belt  of  the  ordinary  oak  tim- 
ber. Still  further  north  again,  prairie  spreads  widely  over  the  limestone  country  of  Court- 
land,  Randolph,  Springdale  and  Scott.  Nearly  all  of  the  country  east  of  the  escarp- 
ment shows  a  most  excellent  soil,  being  underlaid  for  the  most  part  by  limestone,  which 
is,  however,  frequently  buried  beneath  much  glacial  drift.  An  exception  would  be  those 
portions  of  Fountain  Prairie  and  Otsego  where  erosion  has  carried  the  surface  into  the 
horizon  of  the  Madison  sand  beds,  the  result  being  a  loose,  sandy  soil,  like  that  of  the 
regular  Potsdam  regions.  The  streams  watering  this  district  are  mostly  small,  and  all 
flow  eastward  towards  the  Rock  river. 

Immediately  west  of  the  limestone  edge,  there  is  an  abrupt  descent  of  100  to  300 
feet,  and,  beyond,  a  more  gradual  slope  of  50  to  100  feet  to  the  Wisconsin  river.  This 
area  has,  in  general,  the  character  of  a  sandy  plain,  timbered  with  small  oaks,  with 
marshes  along  the  streams,  and  dotted  here  and  there  with  isolated  bluffs,  100  to  400 
feet  high,  from  a  few  acres  to  several  square  miles  in  area,  and  generally  surmounted  by 
a  capping  of  Lower  Magnesian  limestone.  But  very  little  prairie  is  met  with.  Some 
occurs  in  the  town  of  West  Point,  including  both  low  land  and  limestone  outliers.  The 
streams  are  larger  than  those  on  the  east  of  the  divide,  increasing  in  size  as  the  escarp- 
ment recedes  from  the  Wisconsin.  Spring  creek,  in  Lodi,  Okee  creek,  in  southern  De- 
korra  and  northern  Arlington,  Rocky  run,  in  northern  Dekorra  and  Lowville,  the 
several  branches  of  Duck  creek,  in  Pacific,  Wyocena,  Springvale,  Courtland  and  Ran- 
dolph, and  the  Fox  river  in  Fort  Winnebago,  Marcellon,  Wyocena  and  Scott,  are  the 
principal  streams.  The  towns  of  Lewiston,  Newport  and  Fort  Winnebago,  west  of  the 
Fox  river,  and  north  of  the  Wisconsin,  are  similar  to  the  rest  of  this  sand  district  in 
many  respects;  but  are  more  roughened  in  surface,  the  northern  portions  of  the  two  for- 
mer rising  up  to  the  high  land  through  which  the  passage  of  the  Dalles  is  cut. 

West  of  the  Wisconsin  river  we  find  the  topography  influenced  primarily  by  the 
quartzite  ranges  of  the  Baraboo,  which  have  already  been  sufficiently  described.  For 
our  present  purpose  it  is  merely  necessary  to  remember  that  they  are  two  east  and  west 
ranges,  some  twenty  miles  in  length,  uniting  at  both  ends,  and  thus  entirely  enclosing 
the  low  ground  between  them.  They  are  made  up  of  Archaean  quartzite  and  quartz- 
porphyry,  but  the  country  around  and  between  them  is  all  occupied  by  the  horizontal 
formations.  Outside  of  the  ranges  in  the  towns  of  Caledonia,  Columbia  county,  and 
Fairfield,  Merrimack,  Prairie  du  Sac,  and  Sumpter,  Sauk  county,  the  country  is  in  most 
respects  like  the  level  sand  district  immediately  east  of  the  Wisconsin,  showing  in  the 
more  southern  portions  a  few  limestone-capped  outliers.  Farther  west,  however,  we 
pass  beyond  the  western  limit  of  the  glacial  drift,  and  find  the  topography  presenting 
the  usual  marked  change,  being  characterized  by  narrow  ramifying  ridges  and  valleys, 
the  former,  in  the  more  southern  towns,  commonly  capped  by  the  Lower  Magnesian  lime- 
stone, but  in  the  more  northern  formed  entirely  of  sandstone.  In  the  southern  part  of 
Sauk  county,  immediately  west  from  the  drift  limit,  the  ridges  are  found  frequently 
worn  into  narrow,  isolated  crests,  100  to  200  feet  high,  and  with  frequent  rock  exposures, 
constituting  a  very  marked  and  peculiar  scenery.  Farther  west,  the  ridges  are  broader, 
and  large  areas  of  limestone  occur  on  the  higher  levels.  In  the  town  of  Westfield,  west 
from  the  ends  of  the  quartzite  ranges,  the  high  ground  continues,  capped  now  by  the  Lower 
Magnesian  limestone,  and  forming  the  divide  between  Honey  and  Narrows  creeks. 
Honey  creek  enters  the  Wisconsin  about  five  miles  below  Sauk  City.  Following  it  to- 
wards its  source,  we  find  it  separating,  in  the  northern  part  of  the  town  of  Troy,  into 


582  GEOLOGY  OF  CENTRAL  WISCONSIN. 

two  principal  branches,  the  southern  one  setting  back  westward  nearly  parallel  to  the 
Wisconsin,  and  only  about  six  miles  from  it,  the  other  coming  from  the  south  side  of  the 
divide  in  the  town  of  Westfield.  Between  the  wide  valley  of  the  south  branch  and  the 
Wisconsin,  is  a  long  line  of  limestone-capped  bluffs,  which  present  a  bold  front,  200  to 
oOO  feet  high,  along  the  north  shore  of  the  Wisconsin.  North  of  the  Westfield  divide 
the  various  head  streams  of  Narrows  creek  are  found  running  northward,  with  narrow 
und  sharply  defined  intervening  ridges.  Narrows  creek  itself  runs  in  a  level  valley  two 
to  three  miles  wide.  North  of  it,  again,  the  same  narrow  limestone-capped  ridges  are 
found,  until  the  still  broader  valley  of  the  Baraboo  is  reached  in  the  northern  part  of 
Reedsburg.  Beyond  this  again  the  ridgy  topography  continues,  the  ridges  now  alto- 
gether of  sandstone,  and  leading  up  to  the  high  ground  which  forms  the  southern  rim 
of  the  sand  plain  of  Juneau  and  Adams  counties,  and  through  which  the  Wisconsin 
passes  at  the  Dalles.  On  the  slope  towards  the  Dalles,  in  the  northeastern  part  of  Sauk 
county,  the  small  tributary  streams  of  the  Wisconsin  cut  down  through  narrow  rock- 
walled  canons,  similar  to  the  Dalles,  though  on  a  smaller  scale.  The  valley  of  the  Bar- 
aboo, between  the  quartzite  ranges,  is  generally  higher  than  the  country  outside  the 
ranges,  and  is  considerably  roughened  in  surface  by  the  wash  from  the  enclosing  ranges 
towards  the  Baraboo.  The  streams  watering  the  district  west  of  the  Wisconsin  are 
much  larger  than  those  on  the  east  side  of  that  river.  The  largest  of  these  is  the  Bara- 
boo river,  which,  entering  Sauk  county  on  the  northwest,  traverses  it  in  an  easterly  direc- 
tion, passing  between  the  two  quartzite  ranges,  and  reaching  the  Wisconsin  at  the  ex- 
treme eastern  point  of  its  great  bend,  having  in  this  distance  a  fall  of  about  a  hundred 
feet.  Its  numerous  tributary  streams,  dividing  into  many  smaller  branches,  drain  the 
country  for  a  width  of  ten  miles  on  each  side  of  the  river.  South  of  the  southern  quartz- 
ite range  and  of  the  limestone  divide  in  Westfield,  the  only  streams  of  importance  are 
Honey  and  Otter  creeks.  The  former  is  much  the  larger;  separating  into  numerous 
small  branches,  each  with  its  own  ravine,  it  drains  an  area  of  about  185  square  miles. 
Otter  creek  drains  a  considerable  portion  of  the  southern  slope  of  the  main  quart-ate 
range  in  the  town  of  Sumpter,  and  then,  taking  a  due  south  course  towards  the  Wis- 
consin, sinks  into  the  sand  when  within  two  miles  of  the  river.  Except  on  and  about 
the  quartzite  ranges,  the  soil  and  timber  of  the  district  west  of  th^  Wisconsin  follow  the 
same  rule  as  observed  east  of  the  river,  i,  e.,  on  the  lower  levels,  loose  sandy  soils,  whilst 
on  the  higher  limestone  ground,  the  soil  is  clayey  and  excellent.  Good  land,  however,  is 
sometimes  found  on  the  lower  levels,  as,  for  instance,  on  Sauk  prairie,  where  it  is  due 
partly  to  drift  materials;  in  the  town  of  Honey  Creek,  where  stream  detritus  forms 
much  of  the  soil,  and  in  the  northern  part  of  Excelsior,  where  no  such  causes  can  be 
assigned.  Occasional  pine  groves  are  interspersed  amongst  the  ordinary  oak  timber, 
whilst  amongst  the  quartzite  ranges  there  is  a  heavy  growth  of  hard  wood,  largely  maple. 
The  list  of  geological  formations  represented  in  Sauk  and  Columbia  counties  in- 
cludes all  of  the  Central  Wisconsin  formations,  from  the  Archtoan  to  the  Drift,  except 
the  Galena  limestone.  The  Potsdam  sandstone  is  the  surface  rock  over  all  the  lower 
levels  along  the  Wisconsin  and  its  many  tributaries,  besides  forming  considerable  por- 
tions of  the  slopes  of  the  outliers  and  higher  lands.  On  all  sides  of  the  quartzite  ranges  it 
is  found  attaining  very  considerable  altitudes,  apparently  rising  into  the  horizons  of  the 
higher  strata,  whilst  within  the  circuit  of  the  ranges  it  occupies  all  levels,  limestone  being 
found  in  one  or  two  small  patches  only.  Farther  north  again,  in  northern  Sauk  and 
northwestern  Columbia,  it  occupies  all  levels,  having  attained  now  a  much  increased  al- 
titude by  virtue  of  its  general  northern  rise.  The  Mendota  and  Madison  beds  occupy 
parts  of  the  slopes,  or  else  cap  the  summits  of  many  of  the  outliers  that  flank  the  lime- 
stone escarpment  in  Columbia  county,  and  of  the  ridges  of  western  and  south  western 
Sauk.  They  also  form  the  surface  rock  along  the  slope  of  the  western  edge  of  the  lime- 
stone country  of  Columbia  county,  occasionally,  as  in  the  towns  of  Lowville  and  Spring- 


THE  LOWER  SILURIAN  ROCKS. 


583 


vale,  coming  to  the  surface  over  a  belt  of  country  several  miles  in  width.  Even  east  of 
the  limestone  edge,  a  considerable  area  of  the  adjoining  portions  of  Otsego  and  Foun- 
tain Prairie  is  eroded  down  to  the  level  of  the  Madison  sand  beds,  and  yet  surrounded 
entirely  by  the  higher  formations.  Such  an  effect  is  a  peculiar  one,  and  takes  place  only 
where  the  inclination  of  the  surface  bears  such  a  relation  to  the  changing  inclination  of 
the  strata  as  indicated  in  Fig.  37.  The  Lower  Magnesian  limestone  caps  many  of  the 
outlying  bluffs  east  of  the  Wisconsin,  forms  the  summit  of  most  of  the  higher  ridges  in 

FIG.  37. 


r±±\       $"*wr-feUWR5r«rc-  -  - 

2^grg^- --SSSOg^ 


DIAGBASI  SHOWING  HOW  AN  ABBA  o*  A  LOWER  FORMATION  MAY  BE  ENTIRELY  SURROUNDED  BY 

A  HIGHEK  ONE. 

western  and  southwestern  Sauk,  and  is  the  surface  roclfc  nearly  everywhere  in  Columbia 
county,  east  of  the  limestone  edge.  In  this  latter  district,  however,  it  is  overlaid  by  the 
St.  Peters  sandstone  and  Trenton  lime-stone,  in  southeastern  Hampden,  and  southern  Co- 
lumbus, over  a  small  area  in  eastern  Fountain  Prairie,  and  over  a  much  larger  one  in 
northeastern  Courtland  and  eastern  Randolph.  The  St.  Peters  sandstone  occurs  also  in 
several  patches  in  southwest  Arlington,  lying  upon  the  irregular  upper  surface  of  the 
Lower  Magnesian,  and  forms  the  upper  part  of  a  remarkable  bluff  in  the  northeast  part 
of  Weet  Point.  The  characters  of  the  several  formations  arc  indicated  in  the  following 
detailed  descriptions.  Their  thickness,  relative  positions,  etc.,  are  shown  by  the  sections 
of  Plates  XX,  XXII  and  XXIII  of  this  volume,  and  those  attached  to  the  Atlas  Plate  of 
Area  E. 

Beginning  our  detailed  descriptions  in  the  northeastern  comer  of  Columbia  county, 
we  note  first,  on  Sec.  31,  T.  13,  R.  12  E.,  Randolph,  two  quarries  on  the  Mendota  and 
Madison  beds,  on  the  walls  of  a  ravine  at  the  head  of  Duck  creek.  The  quarry  on  the 
west  wall  of  the  ravine  shows  the  following  section: 


MEXDOTA   BEDS. 


I. 


Ft.    In. 


Very  fine-grained,  yellowish-brown,  calcareo-silicious  rock  (1206);  only 
slightly  arenaceous  in  feeling,  but  leaving  a  residue,  on  treatment  with 
acid,  of  69.03  per  cent.,  which  consists  of  exceedingly  fine,  white,  angu- 
lar quartz;  thinly  and  regularly  laminated,  the  layers  running  from  one 

to  four  inches 10     .. 

II.  Very  fine-grained,  close-textured,  yellow-and-purple-blotched,  calcareo- 
argillaceous  rock  (1207);  the  yellow  parts  like  I,  the  dark-colored  a 
sort  of  clay-shale,  occasionally  finely  laminated,  but  not  in  distinct  layers; 
residue  on  treatment  with  acid,  44.53  per  cent.;  layers,  two  to  eight 

inches 6     .. 

III.  Very  fine-grained,  milk-white,  silicious  rock,  without  calcareous  admix- 
ture; non-arenaceous;  similar  to  II  of  next  section 6 


584  GEOLOGY  OF  CENTRAL  WISCONSIN. 

Ft.    In. 
IV.  Similar  to  II 11     . . 

V.  Compact,    yellowish-brown-and-red-blotched,    calcareo-magnesian    rock 

(1210);  differing  from  I  in  having  a  very  fine  crystalline  texture,  and 
cavities  lined  with  dolomite  crystals;  insoluble  residue,  41.73  per  cent.; 
layers  a  foot  thick;  quarry-rock,  used  in  building  at  Cambria  and  other 
places  in  the  vicinity:  obtainable  in  large  well-shaped  blocks 4 

POTSDAM   SANDSTONE. 

VI.  Greensand  layers;  moderately  firm,  rough-surfaced,  brownish,  speckled 

with  green;  calcareous;  leaving  a  residue,  on  treatment  with  acid,  of 
fine,  sharply-angular  quartz,  mingled  with  dark-green  grains 2 

32      6 

The  greensand  appears  without  doubt  to  be  that  generally  recognized  as  marking 
the  base  of  the  Mcndota  horizon,  which  is  here  more  largely  silicious  than  in  the  typical 
localities  in  Dane  county,  though  still  sharply  contrasting  in  character  with  the  Madisoa 
and  Potsdam  sandstone  layers.  A  quarter  of  a  mile  up  the  ravine,  on  ite  east  wall, 
another  small  quarry  opening  shows  the  following: 

MADISON    BEDS. 

feet. 
I.  Fine-grained,  brownish,  ferruginous,  friable  sandstone  (1226);  non-calcareous; 

composed  of  rolled  grains  of  dulled  quartz;  scolithus -bearing 4 

II.  Very  fine-grained,  firm,  pure  white,  silicious  rock  (1212);  composed  of  exceed- 
ingly fine,  sharply  angular  quartz;  non-calcareous;  non-arenaceous;  contain- 
ing 97.52  per  cent,  of  silica;  close  to  III  of  last  section;  upper  layers  shaly . .  3 

MENDOTA  BEDS. 

III.  Similar  to  II,  but  stained  yellow  and  pink  (1213);  very  hard  and  firm;  con- 

taining 98.12  per  cent,  silica 3 

I V.  Reddish-yellow  rock  similar  to  I  of  last  section,  and  apparently  the  same  horizon.      3 

13 

At  P.  Scheasman's  quarry,  on  the  west  line  of  the  S.  W.  qr.  of  Sec.  6,  in  the  same 
town,  a  ten-feet  quarry  face  shows  below,  in  thin  and  very  regular  layers,  a  close- 
textured,  buff-colored,  nearly  pure  dolomite  (1205),  which  weathers  with  a  smooth,  yel- 
lowish surface,  is  marked  finely  with  dendritic  manganese  oxide,  and  is  coated  in  places 
with  white,  stalactitic,  lime  carbonate,  and  at  the  top  a  heavy  layer  of  concretionary, 
dark-colored  dolomite.  On  the  hill  above  are  exposures  of  the  ordinary  rough-textured 
Lower  Magnesian,  near  the  base  of  which  formation  the  quarry  layers  appear  to  lie. 

In  the  railroad  cutting  at  Rio,  in  the  northwest  corner  of  the  town  of  Otscgo,  T.  11. 
R.  12  E.,  the  Madison  and  Mendota  beds  are  exposed.  The  following  is  the  section: 

MADISON    BEDS. 

Feet. 
I.  Brownish,  friable  sandstone 6 

II.  Very  fine-grained,  pure  white,  firm,  silicious  rock;  non-calcareous;  in  upper 
portions  slightly  arenaceous  in  texture  C1219,  close  to  1212);  lower  portions 
without  trace  of  granular  texture;  rough- surfaced  and  pink-tinted  (1216, 
close  to  1213);  bedding  not  distinctly  seen;  composed  of  exceedingly  fine, 
angular  quartz 12 

MENDOTA  BEDS. 

III.  Red-and-yellow-mottled  calcareo-arenaceous  rock 4 

22 


THE  LOWER  SILURIAN  ROCKS. 


585 


I 


2   -2 


Fig.  38  is  a  section  from  south  to  north  along  the  center  line  of 
Sees.  2,  11,  23  and  26,  in  the  town  of  Scott,  T.  13,  R.  11  E.,  and 
serves  to  give  a  correct  idea  of  the  topography  and  stratigraphy 
of  that  township. 

Large  ledges  of  Potsdam  sandstone  rise  on  the  south  side  of  a 
small  creek  in  the  N.  E,  qr.  of  the  N.  E.  qr.  of  Sec.  3,  Arling- 
ton, T.  10,  R.  9  E.,  a  short  distance  south  of   the  village  of 
Poynette.     Here  are  exposed  15  feet  of  white,  heavily-bedded, 
friable,  non-calcareous  sandstone,  with  some  thin  greensand  lay- 
ers, the  base  of  the  ledge  being  60  to  80  feet  below  the  base  of 
the  Mendota  horizon.     Similar  but  higher  ledges  occur  along 
the  creek  in  Pine  Hollow,  in  the  adjoining  pails  of  Sees.  3  and  4. 
The  St.  Peters  sandstone  remains  on  top  of  the  Arlington  prai- 
ne  in  five  isolated  knobs,  the  highest  70  to  100  feet  in  height. 
Three  of  these  are  close  together  on  each  side  of  the  line  between 
Sees.  28  and  29.    The  bluff  on  Spocnam's  land,  N.  E.  qr.  of  the 
S.  E.  qr.  of  Sec.  29,  shows  large  outcrops,  in  a  disturbed  condition, 
of  fine-grained,  friable,  white- and-brown-mottled  sandstone  (725, 
.  726),  composed  of  glassy  quartz  grains,  the  larger  ones  of  which 
g  are  rolled,  the  smaller  ones  angular.     Most  of  the  rock  is  affected 
^  by  a  very  hard,  vitrified  crust,  %  to  %  inch  in  -thickness,  in 
which  the  quartz  grains  appear  to  possess  distinct  crystalline  sur- 
faces.    No  trace  of  calcareous  matter  is  present.     Fine-lamina- 
^  lion  and  cross-lamination  are  plainly  perceptible.    The  knob  on 
«l  Mrs.  A.  D.  Forbes'  land  has  on  the  south  side  a  vertical  cliff,  80 
.2  feet  in  height,  of  similar  but  distinctly  horizontal  and  undisturbed 

• 


(  •':'!«]  *fl  ffl  sandstone.  In  the  S.  "W.  qr.  of  the  S.  W.  qr.  of  Sec.  27,  and  ex- 
3  tending  into  Sec.  28,  and  again  in  the  N.  hf.  of  Sec.  34,  are  other 
similar  bluffs.  On  the  prairie  around  these  sandstone  mounds, 
exposures  of  the  Lower  Magnesian  limestone  are  seen  at  several 
points  whose  elevation  is  greater  than  that  of  the  base  of  the 
sandstone  ledges,  whilst  at  least  two  points,  on  the  south  line  of 
Sec.  21  and  in  the  north  part  of  Sec.  29,  show  the  Limestone  ris- 
ing as  high  as  the  top  of  the  St.  Peters.  The  irregular  nature  of 
the  upper  surface  of  the  Lower  Magnesian  is  thus  distinctly 
proven. 

In  Fort  Winnebago,  T.  13,  R.  9  E.,  the  only  formation  is  the 
Potsdam  sandstone,  which,  in  the  middle  and  western  portions, 
and  again  in  the  southeast,  rises  in  isolated  bluffs.  At  T.  Cough- 
lin's  quarry,  N.  E.  qr.  of  S.  W.  qr.  Sec.  20,  are  exposed  10  feet 
of  heavily-bedded,  fine-grained,  white,  porous,  friable  sandstone 
(741),  which  is  composed  of  glassy,  sub-angular,  quartz  grains, 
and  is  blotched  with  ferruginous  spots.  Rows  of  little  brown- 
stained  pores  mark  the  lamination  very  plainly.  Large  fucoidal 
impressions  occur,  identified  by  Mr.  Whitfield  as  Palceophycus 
duplex,  and  Palcaochoida,  n.  sp.  Large  regular  shaped  blocks  are 
obtained.  The  isolated  bluff  on  the  adjoining  parts  of  Sees.  25 
and  36  shows  numerous  small  exposures  of  white,  crumbling, 
non-calcareous  sandstone,  for  a  thickness  of  about  90  feet.  Fig.  39  is  a  section  from 
this  bluff  across  the  Wisconsin  at  Portage  to  the  quartzite  bluffs  of  Caledonia.  The 
contour  of  the  section  is  copied  from  Gen.  G.  K.  Warren's  report  on  the  Fox  and  Wis- 
consin rivers. 


586 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


In  Lorti  and  Westpoint,  T.  10,  R.  8  E.,  and  T.  10,  R.  7  E.,  rock  exposures  are  very 
frequent  along  the  bluff  sides,  but  only  a  few  prominent  points  can  be  described. 
Kingsley's  bluff,  on  the  edge  of  the  high  country  in  the  N.  E.  qr.  of  Sec.  26,  and  S.  E. 
qr.  of  Sec.  23,  T.  10,  R.  8  E.,  has  the  structure  shown  in  Fig.  40.  The  succession  of 
layers  is  indicated  in  the  following,  beginning  above :  — 

Feet 

I.  Drift- covered  slope  with^ 

out  exposure 20 

II.  Lower  Magnesian  lime- 

stone: in  quarry; 
thin-bedded,  top  gla- 
ciated    5 

III.  Drift- covered  slope: 

without  exposure  . . .  100 

IV.  Madison  sandstone: 

white,  incoherent;  on 
the  edge  of  a  flat 
bench  in  the  hillside.  5 

V.  Mendota  limestone:  yel- 

lowish, regularly  bed- 
d  e  d ,  fine  -  grained; 
containing:  silica, 
44.57;  alumina,  8.68; 
iron  peroxide,  1.18; 
iron  protoxide,  0.22; 
lime  carbonate,2&.()9; 
magnesia  carbonate, 
17.97;  water,  1.28= 
99.83;  exposed  in  a 


i~ 

(22 

•<  _s 
a"  s 

£  53 


3  ..  small  quarry 10 

*•*  o   VI.  Flat  drift-covered  slope 

without  exposure 40 

n  5   VII.  Potsdam  sandstone: 
white,   fine-grained, 
*•  |  loose;    alternating 

g  g  with  harder,  yellow, 

£    _  calcareous    bands; 

£  -3  forming  the  edge  of 

£  *  a  bench 40 

«  .1  VIII.  Steep  slope  without 
exposure,  the  rock 
covered  by  sand  from 
its  own  disintegra- 
tion    90 


Total 


310 


The  Mendota  is  quarried  again 
on  the  side  of  the  hill  just  west 
of  the  depot  at  Lodi,  where  it 
presents  the  typical  yellow  color 
and  reddish  stains,-  and  is  over- 
laid at  the  top  of  the  hill  by 


THE  LOWER  SILURIAN  ROCKS.  587 

white,  incoherent  Madison  sandstone.  Another  and  much  larger  Mendota  quarry  is  oil 
the  south  side  of  the  bluff  in  the  S.  hf  of  Sec.  18,  T.  10,  R.  8  E.  Here  art  some  ten 
feet  of  very  regularly  bedded,  yellow,  sandy  limestone,  the  layers  below  heavy,  above 
thin  and  shaly,  with  fine  large  impressions  of  Dlcellocephalus  Minnesotensis. 

The  very  prominent  isolated  bluff  on  the  N.  E.  qr.  of  Sec.  20,  T.  10,  R.  7  E.,  shows 
the  following  section  at  its  north  end : 

LOWER   MAGNESIAN. 

Feet. 

1.  Grassy  slope,  without  exposure 35 

2.  Coarse,  crumbling,  brownish  sandstone 2 

3.  Slope  without  exposures 18 

4.  Brownish-yellow,  rough,  open- textured  limestone,  somewhat  crystalline;  contain- 

ing cavities  with  calcite  crystals,  numeorous  red  quartzite  pebbles  and  green- 
sand  grains 10 

MENDOTA  AND   POTSDAM. 

5.  Coarse,  brownish  sandstone,  in  perpendicular  ledges 10 

6.  Slope  without  exposure 85 

7.  Friable,  non-calcareous  light-colored  sandstone 15 

8.  Sand-covered  slope  without  exposure 60 

Height  above  road  at  foot 235 

FIG.  40. 
•Section  25   Section  25 


S.I/V.  DiTV&vm  of  Rectum  H.ZTE. 

SECTION  OF  KINOSLET'S  BLUFT,  LODL 

Horizontal  scale  1,0)0  feet  to  1  inch.    Vertical  scale  309  feet  to  1  inch.    Figures  indicate  altitudes 

in  feet  above  Lake  Michigan. 

The  occurrence  of  a  thin  layer  of  non-calcareous  sandstone  within  the  Lower  Magne- 
sian  is  unusual,  but  this  is  not  an  isolated  instance.  The  limestone  No.  4  is  interesting 
because  of  its  similarity  to  the  rock  from  Eiky's  and  Wood's  quarries  in  the  Baraboo 
valley,  the  accurate  determination  of  whose  stratigraphical  position  meets  with  some 
difficulties,  and  because  of  its  somewhat  peculiar  characters  as  compared  with  the 
ordinary  Lower  Magnesian,  the  base  of  which  formation  there  can  be  no  doubt  that  it 
marks.  From  a  similar,  and  equally  prominent  bluff,  on  the  south  side  of  the  samo 
section,  the  profile  of  Fig.  41  is  taken,  running  across  the  Wisconsin  to  the  quartzito 
range  of  Merrimac. 

Gibralter  Bluff  is  the  name  given  to  the  bald  cliff  of  St.  Peters  sandstone  which  sur- 
mounts the  western  end  of  a  large  outlying  area  of  limestone-capped  bluffs,  in  Sees.  17 


588 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


and  18,  T.  10,  R.  8  E.  The  area  over  which  the  sandstone  is  present  is  not  more,  prob- 
ably, than  40  rods  in  diameter,  but  the  top  of  the  bluff  reaches  an  elevation  of  about 
630  feet  above  Lake  Michigan,  or  upwards  of  450  feet  above  the  adjacent  river,  so  that 
it  constitutes  one  of  the  most  striking  points  in  the  scenery  of  this  part  of  the  valley  of 
the  Wisconsin,  rising  far  above  all  of  the  immediately  surrounding  country.  Section  I, 

FIG.  41. 


•4- 


:^^^--  *•— 

SBCTION  ACROSS  THE  VALLIJY  OF  THE  WISCONSIN  IN  WEST  POINT  AND  MBRKIMAC. 

j^  g Line  of  profile.    Horizontal  scale  9-lOths  inch  equals  1  mile.    Vertical  scale,  400  feet  equals 

1  inch. 

of  Plate  XXIII,  and  the  north  and  south  section  attached  to  the  Atlas  Map  of  Area  E, 
show  its  relation  to  the  neighboring  elevations.  Fig.  42  is  a  rough  diagrammatic  sketch 
meant  to  give  some  idea  of  the  character  of  the  western  face  of  this  remarkable  bluff, 
whose  structure  is  further  indicated  by  the  section  of  Fig.  43,  which  is  drawn  to  a  nat- 
ural scale. 

FIQ.  42. 


SKETCH  OF  THE  WESTERN  FACE  OF  GIBRAJ.TER  BLUFF. 
Natural  scale,  1 : 3660. 


THE  LOWER  SILURIAN  ROCKS". 


589 


The  western  face  of  the  bluff  is  precipitous  in  its  upper  portion  for  over  100  feet.  At 
the  top  of  the  cliff  is  a  rounded  summit  composed  in  part  of  glacial  drift,  but  showing 
in  one  place  a  few  broken  layers  of  limestone  (736),  which  are  in  the  proper  position,  and 
have  the  proper  characters  for  the  "  Buff  "  or  Lower  Trenton  limestone.  The  cliff  itself 
is  made  up  of  fine-grained,  light-colored  to  nearly  white,  friable  sandstone  (735),  which 
is  composed  of  angular  and  subangular  quartz  grains,  and  possesses  a  hard,  vitrified 
crust.  In  the  uppermost  parts  of  the  cliff  the  horizontal  bedding  is  distinct,  the  layers 
being  quite  thin;  below,  however,  it  is  not  plainly  perceptible,  whilst  the  whole  has  a 
sort  of  vertically  columnar  appearance,  due  to  jointing.  On  the  upper  part  of  the  long 


FIG.  43. 


Soil  <rnd  Drill 


SECTION  OF  QranALTKu  BLUFF. 

wooded  slope  below,  are  numerous  very  large  sandstone  masses,  evidently  fallen  from 
the  cliff.  At  the  lower  edge  of  this  slope  the  Mendota  limestone  is  partly  exposed,  as 
shown  in  Fig.  43,  and  below  it  the  upper  layers  of  the  Potsdam,  with  intercalated  cal- 
careous "bands.  To  the  right  and  left  of  the  line  of  section,  lower  non-calcareous  sand- 
stone layers  are  exposed,  in  low  cliffs  rising  from  the  edge  of  the  marsh.  At  the  point 
F,  Fig.  42,  on  top  of  a  bare  hill,  only  a  few  rods  from  the  sandstone  cliff,  but  at  an 
elevation  of  40  feet  above  its  base,  is  an  outcrop  of  much  disturbed  Lower  Magnesian 
limestone.  Numerous  points  on  the  surrounding  bluffs  also  show  limestone  at 

elevations  above  the  base  of  the  sandstone 
of  the  Gibralter  cliff,  proving  the  exist- 
ence of  a  very  irregular  upper  surface  to 
the  Lower  Magnesian. 

For  the  district  west  of  the  Wisconsin 
river,  where  both  topography  and  strati- 
graphy are  so  largely  affected  by  the 
quartzite  ranges,  it  will  be  most  suitable 
to  take  up  in  order:  the  area  south  of  the 
the  quartzite  ranges;  that  west  of  the 
ranges;  that  within  them;  and  that  north 
of  them. 

South  of  the  quartzite  ranges.  Fig.  44, 
which  is  a  section  from  the  top  of  the 
quartzite  range  near  the  northwest  cor- 
ner of  Sec.  2.  T.  11,  R.  8  E.,  Caledonia, 

to  the  top  of  a  bluff  in  Dekorra,  serves  to  give  an  idea  of  the  structure  of  this  part  of 

the  Wisconsin  valley .* 
On  the  flanks  of  the  quartzite  in  western  Caledonia,  the  Potsdam  sandstone  rises  to 

altitudes  apparently  in  the  horizon  of  the  Lower  Magnesian,  having  then  a  slight  ap- 


SDCTION  ACROSS  THE  VALLEY  OP  ¥HD  WISCON- 
SIN IK  SOUTHEAST  CALEDONIA. 

Vertical  scale.  350  foet  to  the  inch.    Horizontal 
scale,  154  miles  to  the  inch. 


590  GEOLOGY  OF  CENTRAL  WISCONSIN. 

parent  dip  southward,  or  away  from  the  quartzite.  This  flanking  sandstone  is  well  ex- 
posed at  Dorvrard's  Glen,  on  the  north  side  of  Sec.  18,  where  it  is  seen  overlying  the 
quartzite,  as  heretofore  described  and  illustrated  in  Fig.  27,  which  is  a  section  along  the 
wall  of  the  glen.  This  wall  shows  the  following  succession  of  layers,  the  numbers  of 
the  layers  being  the  same  as  in  Fig.  27 : — 

Ft.    In. 

VI.  Yellowish,  fine-grained,  friable  and  heavily  bedded  sandstone    14      8 

V.  Pink,  fine-grained  and  thinly  bedded  sandstone  4      8 

IV.  Whitish  and  brownish,  very  coarse,  heavily  bedded  sandstone,  the  con- 
stituent grains  much  rolled  translucent  quartz 10 

III.  Similar  to  the  last,  but  yellowish  and  finer  grained 17      4 

II.  Very  coarse,  like  IV. 5    10 

I.  Bowlder-conglomerate,   almost  without  matrix,   made  up  of  bowlders 

mostly  angular,  up  to  1  foot  in  diameter;  forms  the  stream  bed 4      2 

Height  of  cliff 58      8 


In  the  town  of  Merrimac,  Sauk  county,  sandstone  at  high  levels  continues  to  flank 
the  quartzite.  This  sandstone  may  be  seen  at  Parphrey's  Glen,  on  the  N.  E.  qr.  of  Sec. 
22,  T.  11,  R.  7  E..  where  20  feet  of  friable,  brownish,  Scottthus-beaxwg,  regular-bedded 
sandstone  is  exposed,  including  thin  layers  of  a  conglomerate  of  red  quartzite  pebbles; 
on  the  N.  E.  qr.  of  Sec.  28,  in  a  high,  narrow  bluff,  wliich  is  partly  detached  from  the 
quartzite;  and  again,  lying  directly  against  the  quartzite,  on  the  N.  E.  qr.  of  the  S.  E. 
qr.  of  Sec.  20,  T.  11,  R.  7  E.,  where  it  forms  a  perpendicular  cliff  directly  north  of,  and 
across  the  valley  from,  the  Devil's  Nose.  The  rock  at  this  place  is  medium  to  fine- 
grained, friable,  red-and-white-banded,  purely  silicious,  and  superficially  vitrified,  and 
contains  throughout  small  pebbles  of  red  quartzite,  which  are,  however,  aggregated 
more  numerously  into  two  bands,  the  upper  one  2  feet  thick,  and  25  feet  below  the 
summit,  the  lower  one  10  feet  thick  and  59  feet  below  the  summit.  The  whole  height 
of  the  vertical  cliff  is  210  feet,  the  whole  thickness  of  sandstone  seen,  227  feet.  The  top 
of  the  sandstone  has  an  altitude  of  622  feet;  its  base,  one  of  397  feet,  so  that  the  cliff 
rises  entirely  across  the  horizon  of  the  Lower  Magnesian,  as  indicated  by  the  occur- 
rences of  that  formation  in  the  country  to  the  south  east  and  west.  The  sections  of 
Plates  XIX  and  XX  show  the  structure  and  stratigraphical  relations  of  this  cliff. 

The  isolated  knob  rising  from  the  west  bank  of  Otter  creek,  near  the  center  of  Sec. 
15,  T.  10,  R.  6  E.,  Snmpter,  shows  the  following  section: 

Fc,:t. 
I.  Madison  sandstone  in  small  separated  exposures;  upper  portions  very  highly 

ferruginous  and  firm;  near  the  middle  (1227)  very  fine-grained,  lighter 
colored  and  slightly  calcareous;  at  the  base  white,  fine-grained,  much 

indurated „ 25 

II.  Unexposed 20 

III.  Mendota  limestone;  yellow,  shaly,  in  small  quarry-opening 5 

IV.  Unexposed 10 

V.  Grecnsand  layer 1 

VI.  Unexposed .        15 

VII.  Potsdam  sandstone,  upper  layers  fine,  white,  friable,  banded  with  calcareous 

layers,  lower  portions  rising  in  an  abrupt  cliff  from  the  bank  of  Otter 
creek;  heavily  bedded,  non-calcareous,  alternating  brown  and  white 140 

Height  of  knob 216 

Altitude  of  summit .' 415 


PLATE.XX 


I 


THE  LOWER  SILURIAN  ROCKS. 


591 


Fig.  45  is  a  section  across  the  valley  of  the  Wisconsin  from  the  high  bluff  just  west  of 
RowelTs  Mill,  N.  W.  qr.  Sec.  17,  T.  9,  R.  6  E.,  Prairie  da  Sac,  in  a  N.  68°  E.  direc- 
tion to  the  blutf's  back  of  Clifton,  Dane  county. 

Fig.  45. 


SECTION  ACROSS  THE  VALLEY  OP  THE  WISCONSIN,  AT  PRAIRIE  DU  SAC. 
Vertical  scale  400  feet,  1  inch;  horizontal  scale  \y%  miles,  1  inch. 

The  very  bold  and  prominent  bluff  rising  from  the  bank  of  the  Wisconsin  at  the 
mouth  of  Honey  creek,  Sec.  21,  T.  9,  R.  6  E.,  has  already  been  cited  as  giving  a  mag- 
nificent section,  and  portions  of  this  section  have  been  given  in  some  detail  in  the  gen- 
eral descriptions  of  the  formation.  Abbreviated,  the  section  is  as  follows : 

Ft.    In. 
.1.  Lower  Magnesian,  in  a  vertical  cliff  facing  towards  Honey  Creek,  including. 

subdivisions  as  given  on  page  552 52    5 

2.  Madison,  including:  slope  without  exposure,  15  feet;  white  and  brown  sand- 

stone for  the  most  part  non-calcareous,  16.5  feet;  slope  without  exposure, 

7  feet;  coarse,  non-calcareous  white  and  brown  sandstone,  2  feet;  in  all      40    5 

3.  Mendota,  including :  slope  without  exposure,  33  feet;  brown,  earthy,  very  coin- 

pact  limestone  with  34.15  per  cent,  of  white  clay,  1  foot;  like  the  last, 

but  with  26  per  cent,  of  clay,  2^  feet;  in  all 36    6 

4.  Potsdam,  including  subdivisions  as  given  on  page  534;  rising  abruptly  from 

the  Wisconsin , 189    3 

Total  height  of  bluff 318    7 

Altitude  of  summit 484  . . 


HONEY  CREEK  BLUFF 


Fig.  46  is  a  section  across  the  valley  of  the  Wisconsin,  from  the  bluff  just  described, 
in  a  southeasterly  direction  to  the  bluff  on  Sec.  1,  T.  8,  R.  6  E. 

South  of  the  quartzite 

FlG-  46-  range,  over  all  of  T.  10, 

R.  4  E.,  Honey  Creek, 
the  country  is  one  char- 

acterized    by  numerous 

,- 

mgh,  narrow,  branching 

ridges,  which    are.   for 
the  most  part,  severed 


SECTION  ACROSS  THE  WISCONSIN  VALLEY   TROM   IIONEY"   OREEK 
BLUFF. 

Vertical  scale  400  feet  to  the  inch  ;  horizontal,  1V4  miles  to  the  inch. 


parts,  showing  frequent- 

ly walls  of    bare  rock, 

, 
and     often    rising     in- 

to   the    nonzon    of    ^0 
Mendota     beds,     more 


rarely  into  that  of  the  Lower  Magnesian.  In  many  cases,  the  sides  of  tho  ridges  arc 
worn  into  bold  and  fantastic  forms  of  bare  rock,  whose  very  plain  horizontal  stratifica- 
tion renders  the  effect  more  striking.  On  the  N.  W.  qr.  of  Sec.  17,  T.  10,  R.  5  E.,  a 
narrow,  precipitous  spur  from  a  higher  bluff  is  worn  entirely  through,  forming  a  natur»>\ 


592 


GEOLOGY    OF   CENTRAL  WISCONSIN. 


bridge  of  considerable  dimensions.  The  arch  is  about  ten  feet  thick,  its  under  side  being 
30  feet  from  the  ground,  and  the  width  of  the  archway  30  to  40  feet.  The  rock  is  the 
upper  portion  of  the  Potsdam,  containing  the  usual  calcareous  bands,  and  is  highly 
charged  with  small  pebbles  of  red  quarfczite.  The  bases  of  the  cliff's  on  both  sides  of  the 
valley  of  that  branch  of  Honey  creek  which  follows  the  west  line  of  T.  10,  R.  5  E.,  are 
made  up  of  a  layer  50  feet  thick,  of  whito,  non-calcareous  sandrock,  which  is  rendered 
very  prominent  by  its  strong  contrast  in  color  with  the  darker  hued  layers  at  higher 
levels.  Its  upper  surface  appears  to  be  about  155  feet  below  the  Mendota  base,  and  the 
layer  is  evidently  the  same  as  seen  at  the  foot  of  the  great  bluff  at  the  mouth  of  Honey 
creek. 

FIG.  47. 


Slane  WU7unJ  SJ'*^-  '' 
QG  exposure     /*/r  .il 


I&acl 


^   '•--' 


Feet. 


SECTION  OP  RIVTB  BLUFF  NOBTH  op  SPRING 
Horizontal  scale,  235  feet  to  the  inch;  vertical  scale,  100  feet  to  the  inch. 

The  Mendota  is  quarried  on  the  side  of  a  steep  ravine  in  the  river  bluffs  immediately 
north  of  Spring  Green,  N.  W.  qr.  Sec.  3,  T.  8,  R.  4  E.  The  point  of  the  bluff  at  the 
mouth  of  this  ravine  shows  the  profile  and  section  as  indicated  in  Fig.  47.  The  succes- 
sion of  layers,  including  the  quarry  across  the  ravine,  is  as  follows : 

I.  Lower  Magnesian  limestone:  in  numerous  small,  rough-weathered  expo- 
sures; upper  layers  concretionary;  about  midway  of  the  measurement, 
close-textured,  white,  crystalline,  with  chert  and  a  few  dolomite-Lined  cav- 
ities; at  20  feet  above  base,  sandy,  and  including  red  quartzite  pebbles; 
lowest  layers  seen,  brownish,  concretionary,  rough-surfaced,  with  chert  and 
facings  to  the  layers  of  stalactitic  carbonate;  at  base  a  greensand  layer; 

exact  junction  with  the  next  formation  seen 

II.  Madison  sandstone:  in  perpendicular  ledges,  including:  white,  indurated 
sandstone,  with  red  quartzite  pebbles,  13  feet;  loose,  white,  cross-lami- 
nated sand,  7  feet;  unexposed,  about  15  feet;  in  all 

HI.  Mendota  beds:  including:  unexposed,  about  25  feet;  thin,  crumbling, lime- 
stone layers,  b%  feet;  yellow  calcareous  shale  \%  feet:  seven  very  regu- 
lar, heavy,  yellow,  limestone  layers,  with  a  6  inch  parting  near  the  base, 


65 


45 


THE  LOWER  SILURIAN  ROCKS. 


593 


and  capable  of  being  split  into  thin  slabs  (1292)  10^  feet;  unexposed,  10 

feet;  brownish,  red  stained,  porous  limestone,  2  feet;  in  all  about 45 

IV.  Potsdam  sandstone:  including:  greensand  layer,  1  foot:  unexposed,  20 
feet;  white  loose  sand  with  brownish  greensand,  bearing  calcareous  bands 
(1290),  in  a  perpendicular  escarpment,  5  feet;  slope  to  foot  of  bluff  covered 
with  sand,  84  feet;  in  all  about 110 


Height  of  bluff 260 

Altitude  of  summit 465 


West  of  the  western  end  of  the  quartzite  ranges.  The  sandstone  lying  at  high  levels 
about  the  quartzite,  in  the  eastern  part  of  the  town  of  Westfleld,  T.  11,  R.  4  E.,  is,  without, 
doubt,  both  in  and  above  the  horizon  of  the  Lower  Magnesian  limestone,  as  indicated 
by  the  exposures  of  that  roek  to  the  westward.  Half  a  mile  south  of  the  Mendota 
quarry,  on  the  point  of  the  ridge  in  the  E.  hf.  of  Sec.  10,  the  road  crossing  the  same 

FIG.  48. 


Jizndffan  eZieatpej^ 


MAP  AND  SECTION  SHOWING  TUB  RELATIVE  POSITIONS  OP  EIKY'S  LIMESTONE,  AND  THE  SURROUND- 
ING ROCK  EXPOSURES. 
Horizontal  scale  2  miles  to  1  inch.    Vertical  scale  403  feet  to  1  inch.    A  B  C  D,  line  of  section. 

ridge  eastward  is  cut  into  brown,  friable  sandstone,  having  the  proper  position  and 
character  for  the  Madison  beds.  Continuing  eastward,  the  road  rises,  the  ground  be- 
coming full  of  the  cherts  characteristic  of  the  Lower  Magnesian,  but  on  the  southeast 
comer  of  Sec.  10,  non-calcareous,  indurated  sandstone  is  again  in  place,  at  an  elevation 
Wis.  SUB.  — 38 


594  GEOLOGY  OF  CENTRAL  WISCONSIN. 

of  80  feet  above  the  Mendota  in  the  quarry  above  named.  From  this  point,  sandstone 
continues  in  place  as  the  road  ascends  through  the  N.  W.  qr.  of  Sec.  14  to  the  center  of 
that  section,  and  beyond,  reaching  an  elevation  of  250  feet  above  the  Mendota  base. 
The  same  thing  is  to  be  observed  on  the  road  ascending  through  sections  2,  3  and  11  j 
whilst  on  the  eastern  slope  of  the  ridge,  towards  the  valley  within  the  quartzite  ranges, 
sandstone  is  constantly  seen  with  a  great  total  thickness,  lying  within  and  above  tho 
Lower  Magnesian  horizon. 

Within  ilw  quartzite  ranges.  In  the  town  of  Caledonia,  Columbia  county,  more  or 
less  of  Sees.  27,  28,  29,  30,  31,  32  and  33,  T.  12,  R.  8  E.,  lie  between  the  converging 
ranges,  which  unite  on  Sec.  27.  The  area  thus  included  appears  everywhere  to  be  un- 
derlaid by  sandstone,  which  is  of  considerable  thickness.  In  the  northern  portions  of 
Sees.  28,  29  and  30,  the  altitude  is  500  to  550  feet,  as  great  as  that  of  the  northern 
quartzite  range,  and  wells  pass  through  many  feet  of  sandstone,  one  near  the  north 
line  of  Sec.  30  penetrating  170  feet  of  that  rock. 

Along  the  east  line  of  Sec.  25,  T.  12,  R.  7  E.  in  the  town  of  Greenfield,  the 
high  sandstone-filled  countryjust  described  as  occurring  on  the  south  flank  of  the  north 
quartzite  range  in  Caledonia,  breaks  down  suddenly,  in  a  vertical  cliff  135  feet  high,  at 
the  foot  of  which  a  slope  continues  the  descent  to  the  Baraboo  river,  through  an 
additional  vertical  distance  of  275  feet,  and  a  horizontal  distance  of  two  miles.  In 
the  northern  part  of  Sec.  25,  T.  12,  R.  7  E.  on  the  south  flank  of  the  northern 
quartzite  range,  and  within  half  a  mile  of  tins  cliff,  is  a  small  limestone  quarry. 
Fig.  48  gives  a  map  and  section  showing  the  relative  positions  of  this  limestone  and 
the  other  rock  exposures  in  the  vicinity.  The  whole  thickness  of  limestone  exposed 
is  about  25  feet,  the  layers  running  from  1  to  6  inches,  but  much  displaced,  and  cov- 
ered by  debris.  The  rock  (1251)  is  rough-textured,  brownish-yellow,  and  non-arena- 
ceous, carrying  many  small  cavities  lined  with  calcite  crystals,  as  also  much  greensand 
in  coarse  grains;  these  much  more  abundant  in  the  lower  layers,  at  the  base  of 
which  is  a  regular  greensand  layer  such  as  is  often  to  be  seen  at  the  base  of  the 
Lower  Magnesian.  The  composition  of  the  limestone  is  indicated  by  the  following 
analysis,  made  gratuitously  for  the  survey  by  Mr  W.  A.  Hover  at  the  State  Uni- 
versity: lime  carbonate,  51.61;  magnesia  carbonate,  38.51;  silica,  5.66;  alumina  and 
iron  oxide,  2.26;  water,  0.40.  The  uppermost  layer  in  the  quarry  is  finely  glaciated, 
and  casts  of  fossils  are  found  throughout.  The  following  have  been  identified  by 
Mr.  R.  P.  Whitfield,  from  a  collection  made  at  this  place  by  the  late  Prof.  James 
H.  Eaton:  Stromatopor'a,  und.  sp.;  Orthis  Barabuensis?  ;  Metoptoma,  n.  sp.;  Mac- 
lurea  Sivezeyi,  n.  sp.;  Holopea,  n.  sp.;  lllcenus  antiquatus,  n.  sp.;  Dicellocephalus 
Barabnetisis,  n.  sp.  Immediately  above  the  quarry,  the  ground  rises  rapidly  to 
the  northward  for  60  feet,  without  exposure;  becoming  then  nearly  level  on  top  of 
the  quartzite  range.  A  short  distance  along  the  road  which  ascends  to  the  eastward, 
are  small  exposures  (  "  a"  of  the  map  of  Fig.  48,  corresponding  in  elevation  to  "a11 
of  the  section)  of  brownish,  non-calcareous,  sandstone,  20  feet  higher  than  the  top 
of  the  quarry.  Down-hill,  a  short  distance  to  the  westward,  are  ledges  of  fine- 
grained, friable,  light-colored,  non-calcareous,  sandstone  (746)  coming  immediately 
below  the  quarry  layers,  some  ten  feet  in  height;  whilst  still  farther  west,  sandstone  ex- 
posures are  seen  at  different  levels  (b,  c,  of  Fig.  48),  down  to  140  feet  below  the  quarry 
base,  but  not  continuously.  The  base  of  the  sandstone  cliff  lying  half  a  mile  southeast 
across  the  intervening  valley,  is  75  feet  above  the  top  of  the  quarry  layers.  Its  lower 
layers  (748)  are  medium-grained,  veiy  friable,  brownish,  banded  sandstone,  composed  of 
very  much  rolled  quartz  grains;  further  up,  some  bands  of  bright  red  sandstone  are  in- 
cluded, whilst  near  the  summit  (740,  750)  are  a  number  of  rapidly  alternating,  red, 
white,  and  yellow  bands  of  quite  fine-grained  and  saccharoidal  sandstone,  the  whole 
thickness  being  135  feet.  The  determination  of  the  true  stratigraphical  position  of  tho 


THE  LOWER  SILURIAN  ROCKS. 


595 


Eiky  limestone  meets  with  considerable  difficulties,  and  has  quite  important  conclusions 
depending  upon  it.  This  subject  is  discussed  briefly  in  another  place,  in  connection 
with  facts  from  other  localities  bearing  on  the  same  conclusion.  It  is  only  necessary 
to  say  here  that  the  fossils  from  this  limestone  are  regarded  by  Mr.  Whitfield  as  cer- 
tainly not  lower  than  the  Lower  Magnesian,  and  that,  if  we  receive  this  reference,  it 
becomes  necessary  to  believe  that  the  surrounding  high-level  sandstone,  apparently 
without  doubt  of  the  Potsdam  series,  had  been  extensively  eroded  before  the  deposition 
of  the  limestone,  and  that  the  latter  forms  merely  a  nest  lying  upon  the  -eroded  surface 
of  the  older  sandstone,  as  indicated  by  the  dotted  line  of  Fig.  48. 

Sandstone  is  quarried,  of  excellent  quality,  at  several  places  near  Bare  boo.  One  of 
these  is  on  the  south  side  of  a  ridge  on  the  N.  E.  qr.  of  Sec.  1,  T.  11,  R.  6  E.,  just  east 
of  the  village.  The  quarry  here  has  a  six-feet  face,  showing  heavy  and  regular  beds  of 
moderately  fine-grained,  white,  non-calcareous  sandstone  (1230),  which  is  marked  with 
fine  brownish  lamination  lines,  is  made  up  of  glassy,  subangular  quartz  grains,  and 
splits  easily  into  thin  slabs.  Another  and  much  larger  quarry  is  opened  on  the 
"  stossed  "  point  of  a  ridge,  southwest  of  Baraboo,  on  the  N.  E.  qr.  of  Sec.  2,  T.  11,  R. 
6  E.  The  end  of  the  ridge  is  planed  and  scratched  on  a  large  scale.  The  total  thick- 
ness seen  is  about  thirty  feet,  the  sandstone  being  white,  fine-grained,  firm,  and  obtain- 
able in  large,  well-shaped  blocks.  In  places,  a  net- work  of  thin  quartz  seams  is  notice- 
able. This  stone,  as  well  as  that  quarried  at  other  points  in  the  Baraboo  valley,  is  an 
unusually  good  sandstone  to  come  from  the  Potsdam,  series,  much  of  which  is  so  loose- 
and  friable,  or  badly  colored,  as  to  have  no  value  as  a  stone  for  building. 

FIG.  49. 


MAP  AND  SEJTION  SHOWING  THE  KELATIVB  POSITIONS  OF  TIIE  EOCK  OUTCROPS  AT  WOOD'S,  NKAR 

BARABOO. 

On  the  N.  W.  qr.  of  the  S.  W.  qr.  of  Sec.  10,  T.  11,  R.  6  E.,  on  Mr.  Joseph  W. 
Wood's  land,  is  a  small  quarry,  on  the  point  of  a  ridge,  of  limestone  closely  like  that  at 
Eiky's  quarry  in  Greenfield.  The  rock  (1260)  is  brownish,  porous,  rough-surfaced,  and 
minutely  crystalline,  with,  in  places,  a  concretionary  structure,  and  contains  only  9.03 
pec  cent,  of  insoluble  ingredients,  which  are  aluminous  rather  than  silicious.  In  places 
an  indistinct  columnar,  coral-like  structure  is  noticeable,  but  no  undoubted  fossils  were 
observed.  On  the  south  face  of  the  same  ridge,  and  on  the  south  line  of  Sec.  10,  is  a 
long  ledge  of  fine-grained,  reddish-brown  sandstone  (1262),  which  is  composed  of  rough- 
surfaced.  subangular  grains  of  glassy  quartz,  and  contains  many  pebbles  of  red 
quartzite.  numerous  Scolithus  borings,  and  fine,  large  impressions  of  Dicellocephalus 


5D6  GEOLOGY  OF  CENTRAL  WISCONSIN. 

Minnesotensis.  The  top  of  this  sandstone  ledge  is  on  a  level  with  the  base  of  the  lime- 
stone in  Wood's  quarry,  directly  beneath  which  a  small  exposure  of  smilar  sandstone  is 
seen.  South  of  the  sandstone  ledge,  on  the  south  line  of  Sec.  10,  as  shown  on  the  map 
and  section  of  Fig.  49,  is  the  valley  of  Skillet's  creek,  and  south  of  this,  again,  rises  the 
southern  quartzite  range.  About  %  mile  north  from  Wood's  quarry,  and  40  feet  be- 
low its  base,  in  the  high  bank  of  Skillet's  creek,  is  an  exposure  of  yellowish,  rough-sur- 
faced limestone  (1263),  which  closely  resembles  the  typical  Mendota  rock,  leaving  on 
solution  23.68  per  cent  of  a  very  fine  aluminous  residue.  The  exposure  is  somewhat 
broken,  but  a  thickness  of  about  15  feet  is  seen.  At  the  foot  of  the  bank,  sandstone  is 
in  place.  This  yellowish  limestone  would  appear  to  he  the  rock  alluded  to  by  Dr.  B.  F. 
Shumard  in  Owen's  Geological  Survey  of  Wisconsin,  Iowa  and  Minnesota,  p.  522,  as 
occurring  "  in  the  bank  of  a  small  stream  %ths  of  a  mile  south  of  the  Baraboo."  He 
refers  it  to  the  "  cncrinital  bed  of  F.  I,"  the  same  as  the  Mendota  horizon  of  the  writer's 
reports.  It  will  be  noticed  that  the  quarry  limestone,  the  sandstone  carrying  Scolitlms 
and  Dicelloceplialus,  and  the  yellowish  limestone  on  Skillet's  creek,  have  the  proper  re- 
lations and  characters  for  the  Lower  Magnesian,  Madison  and  Mendota  beds.  The  up- 
per limestone  has  just  about  the  same  altitude  as  that  at  Eiky's  quarry,  and  appears 
beyond  question  to  belong  to  the  same  horizon.  Below  the  Mendota  normally  there  is 
always  found  loose,  fine-grained  sandstone,  with  some  calcareous  matter,  and  narrow, 
brownish,  calcareous  bands,  this  character  holding  for  a  thickness  of  40  to  60  feet.  Be- 
low the  lower  limestone  on  Skillet's  creek,  however,  we  find  no  such  layers,  but  at  the 
falls,  a  few  rods  down  stream,  are  seen  fifteen  feet  of  very  regular  beds  of  much  in- 
durated, entirely  non-calcareous,  sandstone  having  a  slight  slant  southward,  and  bear- 
ing no  resemblance  whatever  to  the  ordinary  infra-Mendota  layers.  Do  the  two  lime- 
stone layers,  with  the  intervening  sandstone,  form  a  patch"  lying  upon  an  eroded  surface 
of  much  older  sandstone,  represented  by  the  indurated  rock  at  the  falls,  as  suggested 
already  in  the  case  of  the  limestone  of  Eiky's  quarry? 

A  short  distance  northeast  of  Devil's  Lake,  on  the  east  line  of  the  N.  E.  qr.  of  Sec. 
13,  T.  11,  R.  6  E.,  on  the  south  flank  of  a  projecting  point  of  the  south  quartzite  range, 
are  numerous  large  masses  of  fossiliferous  sandstone,  evidently  near  home.  The  rock 
is  medium-grained,  friable  and  brownish,  containing  many  Scolithus  markings,  and 
other  fossil  fragments,  chiefly  of  trilobites,  among  which  casts  of  large  cephalic  shields 
of  Dicelloceplmlus  Minnesotensis  are  most  readily  made  out.  Prof.  A.  Winchell  iden- 
tified and  described  also  the  following, 'in  specimens  from  this  place,  sent  him  a  number 
of  years  ago:  Orihis  Barabuensis;  Stramrollus  (Ophileta)  primordialis ;  Phurotoma- 
ria?  advena;  Dicellocephalus  Pepinensis;  Ptycliaspis  Barabuensis.  The  altitude  at 
which  these  sandstone  masses  occur  is  5'ZO  to  560  feet,  or  70  to  110  feet  above  the  lime- 
stone at  Wood's  and  Eiky's  quarries,  and  110  to  155  feet  above  the  Mendota-like  rock 
in  the  banks  of  Skillet's  creek,  Sec.  10,  T.  11,  R.  6  E.  Across  the  ravine  on  the  north 
side  of  which  these  fossils  are  found,  are  bowlder-conglomerate  and  sandstone  beds  seen 
lying  directly  upon  the  quartzite,  as  previously  described  and  figured.  These  occur  at 
the  north  point  of  the  east  cliff  of  Devil's  Lake,  a  north  and  south  section  through 
which  is  given  on  Plate  XIX  of  this  volume.  The  summit  of  the  cliff,  which  for  some 
distance  is  a  mere  crest,  rises  rapidly  southward,  horizontal  sandstone  layers  flanking  it 
on  the  side  away  from  the  lake,  and  rising  with  it  to  an  altitude  of  over  600  feet.  The 
sandstone  cliff  immediately  opposite  the  Devil's  Nose,  shown  also  in  one  of  the  sections 
of  Plate  XIX,  has  already  been  described  as  extending  between  the  altitudes  of  391 
and  622  feet,  or  from  50  feet  below  Wood's  quar  y,  to  175  feet  above  it,  and  as  ex- 
tending far  above  any  apparently  possible  horizon  of  the  Lower  Magnesian.  The  same 
appears  to  be  true  of  the  sandstone  in  all  of  the  region  about  Devil's  .Lake.  At  the 
south  end  of  the  west  bluff,  for  instance,  are  horizontal  sandstone  ledges  at  an  altitude  of 
over  700  feet. 


PLATE.XXIV 


THE  LOWER  SILURIAN  ROCKS.  597 

On  the  eastern  side  of  the  north  and  south  quartzite  range  in  \Vestfield,  T.  11  R.  4 
E.,  in  the  eastern  row  of  sections  of  that  town,  sandstone  similar  to  that  just  described 
occurs  with  a  considerable  thickness.  Certain  layers  at  high  levels  are  peculiar  in  being 
charged  with  the  red  and  brown  oxides  of  iron,  which  are  at  times  in  quantity  sufficient 
to  constitute  an  iron  ore.  This  ore  is  to  be  seen  in  a  pit  on  F.  W.  Schulte's  land,  S.  W. 
qr.  of  the  S.  E.  qr.  of  Sec.  13,  with  a  thickness  of  about  10  feet.  It  is  plainly  stratified, 
and  is  a  more  or  less  sandy  admixture  of  the  red  and  brown  oxides  of  iron,  the  former 
occasionally  showing  metallic  surfaces,  and  greatly  predominating.  The  inner  part  of 
the  purer  fragments  presents  a  dark-colored,  compact  appearance,  yielding  a  red  streak. 
Occasional  stalactitic  portions  are  to  be  seen,  and  some  of  the  layers  are  almost  without 
iron  oxide,  consisting  then  of  greyish  sand  with  some  greensand  (glauconite)  grains. 
The  following  analysis  (1269)  is  from  a  sample  averaged  from  the  ore  pile  outside,  and 
covers  all  degrees  of  richness  except  the  nearly  pure  sandstone  layers:  Silica,  19.59; 
alumina,  3.60;  iron  sesquioxide,  70.24;  manganese  oxide,  0.54:  lime,  0.76;  magnesia, 
0.04;  phosphoric  acid,  0.17;  sulphur,  a  trace;  water,  5.19  =  100.33:  metallic  iron,  49.30. 
Much  of  the  ore  of  the  pile  is  better  than  shown  by  the  analysis,  which  itself  represents 
an  ore  of  some  value..  The  locality  is  worthy  of  close  investigation,  the  indications  be- 
ing that  a  considerable  quantity  of  a  good  "soft  hematite  "  might  be  obtained. 

North  of  the  quartzite  ranges  the  Potsdam  is  everywhere  the  surface  rock,  making 
frequent  exposures,  many  of  which  are  very  interesting,  but  the  space  is  not  available 
for  their  description.  / 

' '  /    / 
DANE  OoUHTT.  [   />   /> 

f'\  'l    i 

(ATLAS  PLATE  XIII.    AHEAD.)  '»'/  *    /•* 

•/''/'  1 

Dane  is  one  of  the  largest  counties  in  the  settled  portions  of  the  state,  lyivamj  a  total  »',S'  /  , 

area  of  1,237.84  square  miles.    Its  shape  is  that  of  an  almost  perfect  rectaag/e,  khe 
northwestern  corner  of  which  is  cut  off  by  the  Wisconsin  river.     From  north  to  soutunt  ( Jj  » 
measures  30  miles,  including  towns  5,  6,  7,  8  and  9;  from  east  to  west,  42  miles,  includ-         '  v\  /    ., 
ing  ranges  6,  7,  8,  9,  10,  11,  12;  thus  embracing  34  entire  townships  and  one  fractional  f  . 

one.  The  western  tier  of  townships,  range  6,  is  included  within  the  area  of  the  lead 
region,  and  will  be  found  described  in  the  report  of  Mr.  Moses  Strong.  The  balance  of 
the  county  has  an  area  of  1,030  square  miles. 

Dane  county  has  a  position  just  about  midway  in  the  width  of  the  state,  its  eastern 
line  being  57  miles  from  Lake  Michigan,  and  its  western,  63  miles  from  the  Mississippi. 
Its  southern  line  is  24  miles  north  of  the  Illinois  state  line. 

With  the  exception  of  an  area  of  about  120  miles,  in  the  northwest,  that  drains  toward.? 
the  Wisconsin,  the  drainage  of  the  whole  county  is  shed  southward  and  eastward 
through  different  channels  into  Rock  river.  This  result  is  due  to  the  fact  that  nearly 
the  whole  area  lies  on  the  south  side  of  the  limestone  dividing  ridge  that  limits  the  val- 
ley of  the  Wisconsin  on  the  south.  This  ridge  enters  the  county  on  the  north  side  of 
the  town  of  Vienna,  trends  thence  south  of  west  across  Dane,  and  then,  bending  more 
to  the  south,  passes  through  the  adjoining  portions  of  Roxbury,  Berry,  Springfield,  Mid- 
dleton  and  Cross  Plains,  and  leaves  the  county  on  the  west  side  of  the  last  named  town. 
The  ridge  has  a  general  altitude  of  500  to  600  feet,  and  a  width  sometimes  of  a  whole 
township,  but  on  both  sides  is  rendered  quite  irregular  by  erosion,  the  northern  side 
especially  projecting  in  long,  bold  points  into  the  valley  of  the  Wisconsin.  The  summit 
of  the  ridge  is  largely  occupied  by  prairie —  a  continuation  of  the  prairie  belt  that  char- 
acterizes the  same  ridge  in  its  passage  across  Columbia  county  —  and  has  always,  except 
in  Middleton  and  Cross  Plains,  the  Lower  Magnesian  as  the  surface  rock.  In  these 
towns  it  rises  into  the  St.  Peters  and  Trenton  horizons.  In  the  northern  portions  of 
Middleton,  Cross  Plains,  Berry  and  Mazomanie  the  dividing  ridge  is  cut  entirely  through 
by  a  valley  half  a  mile  to  a  mile  in  width,  18  miles  in  length,  and  100  to  200  feet  in 


598  GEOLOGY  OF  CENTRAL  WISCONSIN. 

depth  —  which  connects  the  ground  about  the  west  end  of  Lake  Mendota  with  that 
bordering  the  Wisconsin.  The  highest  point  of  the  valley  is  85  feet  above  Lake  Meii- 
dota,  and  in  it  are  streams  running  in  either  direction.  Black  Earth  river  —  the  larger 
of  the  two  —  which  runs  westward  to  the  Wisconsin,  heads  within  three  miles  of  Lake 
Mendota,  and  at  only  80  feet  above  its  level.  It  has  been  suggested  by  Gen.  G.  K. 
Warren  in  his  report  on  the  Fox  and  Wisconsin  rivers,  that  this  valley  indicates  a  former 
outlet,  westward  to  the  Wisconsin,  of  the  Madison  system  of  lakes.  It  is  not  impossible 
that  such  an  outlet  may  have  existed,  but  there  is  nothing  in  the  structure  of  the  region 
to  show  that  we  have  here  anything  else  than  a  case  where  two  systems  of  erosion  have 
approached  one  another  until  the  dividing  ridge  has  been  partially  broken  clown.  South 
of  Black  Earth  river  the  high  ground  comes  in  again,  and,  taking  a  turn  westward  to 
accord  with  the  changed  direction  of  the  Wisconsin  river,  passes  out  of  the  district. 

To  the  north  and  west,  in  the  towns  of  Dane,  Roxbury  and  Berry,  the  dividing  ridge 
presents  a  very  abrupt  escarpment,  which  projects  in  long  bold  points  into  the  valley  of 
the  Wisconsin.  Beyond  the  escarpment  the  low  ground  is  occupied  by  numerous  out- 
lying patches  of  the  high  country  of  varying  sizes,  similar  to  those  already  described  as 
occurring  in  the  adjoining  towns  of  West  Point,  Lodi,  etc.,  in  Columbia  county. 

Southward  from  the  dividing  ridge  there  is  a  general  and  much  more  gradual  descent  to 
the  south'  and  east,  conforming  with  the  descent  in  those  directions  of  the  underlying 
strata.  West  of  a  line  drawn  centrally  north  and  south  through  the  county,  the  general 
descent  of  both  the  country- surface  and  strata  is  southward  only.  East  of  such  a  line, 
the  line  of  greatest  descent  veers  more  and  more  to  the  eastward,  until  along  the  north- 
ern part  of  the  east  line  of  the  county,  it  is  almost  wholly  in  that  direction.  The  drain- 
age system  corresponds  with  this  general  structure.  In  the  northeast,  in  the  towns  of 
York,  Bristol,  Sun  Prairie  and  Medina,  the  drainage  is  eastward  into  Waterloo  creek. 
Farther  south,  in  Cottage  Grove,  Deerfield  and  Christiana,  the  drainage  is  also  eastward 
towards  Koskonong  creek,  which  itself  has  a  general  southerly  direction.  In  the  central 
part  of  the  county  the  drainage  along  the  Catfish  valley  is  in  a  southeasterly  direction, 
whilst  farther  west,  the  Sugar  river  system  runs  almost  exactly  southward.  In  minor 
detail,  of  course,  the  directions  of  the  streams  are  due  to  other  causes. 

The  Catfish  valley,  with  its  chain  of  lakes,  is  the  central  topographical  feature  of  the 
county.  The  head- waters  of  the  Catfish  are  a  number  of  small  streams  which  rise  on 
the  south  side  of  the  divide  in  Springfield,  Dane,  Vienna  and  Windsor,  and  coine  to- 
gether in  the  southern  part  of  the  town  of  Westport.  From  here  to  the  junction  with 
Rock  river,  the  valley  has  a  southeasterly  course,  a  length  of  27  miles,  and  a  width  from 
high  ground  to  high  ground  of  from  4  to  9  miles.  Its  surface  lies  generally  at  from  250 
to  300  feet  above  Lake  Michigan,  but  is  quite  irregular,  the  irregularity  being  largely 
due  to  considerable  accumulations  of  drift,  but  also  to  the  occurrence  of  small  rock  out- 
liers, and  to  the  projection  into  the  valley  on  either  side  of  low  rock  ridges.  These  have  a 
general  northeast  southwest  trend,  and  tend  to  divide  the  valley  into  more  or  less  sepa- 
rate, parallel,  cross-valleys,  which  are  very  marked,  and  are  undoubtedly  to  be  attrib- 
uted to  the  movement  over  the  country  of  glacier  ice,  to  which  cause  also  is  to  be  assigned 
the  linear  nature  of  the  topography  of  all  of  the  eastern  part  of  the  county.  The  several 
lakes  of  the  region  about  Madison  are  expansions  of  the  Catfish  into  such  cross-valleys, 
the  ridges  between  which  here  run  entirely  across  the  main  valley,  though  not  formed 
throughout  of  rock  material.  Lake  Mendota  occupies  two  of  the  cross-valleys,  partially 
separated  by  the  low  ridge  of  Picnic  point  and  McBride's  point.  Lake  Monona  lies  m 
one  similar  valley,  which  extends  far  to  the  southwestward,  and  holds  also  the  smaller 
sheet  of  water  known  as  Dead  Lake,  or  Lake  Wingra.  Further  south,  the  glacial  move- 
ment had  a  more  nearly  southerly  direction,  and  the  directions  of  the  cross- valleys  cor- 
respond. There  is  no  prairie  in  the  Catfish  valley  proper.  Along  the  head  streams  in 
Springfield,  Westport  and  Burke,  the  marshes  are  of  considerable  extent. 


THE  LOWER  SILURIAN  ROCKS.  599 

Immediately  east  of  the  Catfish  valley  the  country  lies  higher,  but  soon  sinks 
again,  descending  with  the  eastward  descent  of  the  strata,  this  part  of  the  county  run- 
ing  from  240  to  400  feet  in  altitude.  Here  we  find  a  gently  undulating  surface,  the 
ridges  having  a  flowing  contour,  and  all  topographical  features  showing  the  linear  di- 
rection induced  by  the  glacial  movement.  Numerous  narrow  and  linear  marsh  strips 
are  found  on  the  lowest  portions,  whilst  prairies  of  some  size  occur  on  the  highest,  be- 
ing for  the  most  part  underlaid  by  limestone. 

On  the  west  side  of  the  Catfish  valley  is  a  high  and  hilly  belt  of  country  from  400  to 
600  feet  in  altitude,  which  extends  southward  from  Middleton,  along  the  adjoining 
parts  of  Verona,  Fitchburg,  Oregon  and  Montrose.  Crossing  the  divide  in  the  Sugar 
river  valley,  we  find  ourselves  in  an  entirely  different  looking  country  —  one  where  all 
irregularities  are  due  solely  to  subaerial  erosion,  where  the  ridges  are  high  and  bold,  and 
the  branch  valleys  ramifying,  narrow,  and  steep-sided.  The  two  main  branches  of 
Sugar  river  separate  on  the  southern  line  of  the  town  of  Montrose,  one  setting  back  in 
a  more  westerly  direction  than  the  other.  Both  have  numerous  branch-streams,  each 
of  which  has  its  steep-sided  flat- bottomed  ravine.  Here  the  ridges  rise  to  500  or  600  feet 
in  altitude,  and  are  nearly  always  occupied  by  fertile  prairie,  whilst  the  valley  bottoms 
stand  at  300  to  400,  are  wooded  with  a  growth  of  small  oaks,  and  show,  rarely,  narrow 
strips  of  marsh. 

As  to  fertility  of  soil,  Dane  ranks  as  one  of  the  best  counties  in  the  state.  The 
prairies,  found  for  the  most  part  on  the  higher  ground,  owe  their  especial  fertility,  usu- 
ally, to  the  underlying  limestone,  but  the  low  ground  of  the  Catfish  valley,  though  often 
on  the  upper  sandy  layers  of  the  Potsdam  series,  has  everywhere  an  excellent  soil,  which 
it  owes  to  alluvial  depositions,  or  to  the  drift  materials.  A  poor  soil  is  seen  only  on  the 
low  grounds  adjoining  the  Wisconsin  river,  where  the  sand  comes  from,  the  Potsdam 
sandstone.  The  St.  Peters  sandstone  rarely  affects  the  soil  over  any  considerable  area. 
East  of  the  drift  limit,  it  is  buried  beneath  drift  materials,  whilst  west  of  the  same  line 
it  appears  only  on  the  steep  sides  of  ravines.  The  prevailing  timber  of  Dane  county  is 
email  oak,  occurring  in  patches  or  groves,  constituting  what  are  known  as  "oak  open- 
ings." 

The  Dane  county  list  of  geological  formations  includes  nearly  the  whole  Wisconsin 
series.  The  Cincinnati  and  Niagara,  however,  occur  only  on  the  Blue  Mounds,  and  in 
that  portion  of  the  county  that  is  not  included  in  the  Central  Wisconsin  district. 

The  Arcncean  does  not  come  to  the  surface  in  Dane  county,  but  the  Artesian  borings 
at  Madison  reach  it  at  some  800  feet  below  the  surface,  and  480  feet  below  the  level  of 
Lake  Michigan,  at  winch  point  a  dark-grey  felsitic  rock  is  -struck.  Into  this  one  of  the 
wells  penetrates  for  187  feet,  reaching  a  point  667  feet  below  Lake  Michigan,  and  82 
below  the  level  of  the  sea.  The  Potsdam  sandstone  comes  to  the  surface  along  the  val- 
ley of  the  Wisconsin,  and  along  the  bottoms  of  a  number  of  smaller  tributary  valleys  in 
Dane,  Roxbury,  Berry  and  Cross  Plains.  It  is  also  at  the  surface  over  a  considerable 
area  at  the  head  of  the  Catfish  valley,  and  in  the  bottoms  of  branch  valleys,  in  Spring- 
field, Westport,  Windsor,  Burke,  etc. ;  but  in  all  this  area  only  the  uppermost  layers  of 
the  formation  are  at  surface.  The  Mendota  and  Madison  beds  are  the  surface  rocks  over 
a  large  portion  of  the  Catfish  valley,  reaching  from  the  south  side  of  Lake  Monona  to 
the  south  side  of  Lake  Kegonsa.  These  layers  are  at  surface  along  some  of  the  valley- 
bottoms  of  northern  Middleton,  southern  Springfield,  and  adjoining  towns,  as  also  on 
the  flanks  of  the  higher  ground  and  outliers  that  border  the  valley  of  the  Wisconsin. 
The  total  thickness  of  the  two  layers  in  Dane  county  is  about  70  feet.  The  Lower  Mag- 
nesian  limestone  forms  the  upper  part  of  all  the  dividing  ridge  of  the  north  part  of  the 
county.  It  fo  ms,  also,  the  flanks  of  the  high  ground  on  both  sides  of  the  Catfish  valley, 
whose  bottotb  *t  becomes  in  the  region  south  of  Lake  Kegonsa.  It  comes  up  again  un- 
derneath tno  o,v  marshy  ground  that  borders  Waterloo  creek  in  York,  Bristol,  Sun 


600  GEOLOGY  OP  CENTRAL  WISCONSIN. 

Prairie  and  Medina,  its  eastward  descent  having  carried  it  here  far  below  the  altitudes 
at  which  it  is  found  on  the  west  side  of  the  county.  It  lies  also  at  the  bottom  of  the 
valley  of  Sugar  river  and  its  numerous  branch  valleys,  crowns  the  outlying  bluffs  of  the 
Wisconsin  valley,  and  occurs  also  in  several  small  isolated  patches,  within  the  Potsdam 
area  of  the  Catfish  valley.  The  thickness  of  the  Lower  Magnesian  in  Dane  county  seems 
rarely  to  be  more  than  80  feet,  whilst  its  very  irregular  upper  surface  brings  it  often  into 
the  horizon  of  the  next  formation  above.  The  St.  Peters  sandstone  occupies  a  large 
tract  on  the  east  side  of  the  Catfish  valley,  where  it  appears  to  be  never  more  than  50 
feet  in  thickness.  It  is  found,  also,  forming  a  narrow  band  around  the  Trenton  areas 
of  York,  Bristol  and  Windsor.  West  of  the  Catfish  valley  it  occupies  much  of  the  high 
ground  forming  the  divide  from  the  valley  of  the  Sugar  river.  In  the  last-named  valley 
and  its  branches  the  St.  Peters  forms  the  lower  part  of  the -bluff  sides,  having  its  full 
thickness  of  80  to  90  feet.  It  occurs  also  in  several  detached  areas  in  the  high  country 
north  of  Black  Earth  creek.  The  Trenton  limestone  occurs  in  detached  areas,  mostly  of 
considerable  size,  capping  the  high  ground  on  both  sides  of  the  Catfish  valley.  Some  of 
the  areas,  however,  are  quite  large,  covering  one  or  two  townships,  as  in  Middleton, 
York,  Christiana  and  Albion.  In  Springdale  and  Primrose  the  narrow  ridges  between 
the  streams,  carry  the  whole  thickness  of  the  Trenton  limestone,  being  at  times  capped 
by  the  Galena.  For  the  most  part,  the  Trenton  areas  of  Dane  county  include  only  the 
lower  part  of  that  formation.  The  Galena  limestone  occurs  only  as  a  capping  on  tho 
higher  parts  of  the  ridges  of  Springdale  and  Primrose,  and  in  two  or  three  small  areas 
in  Christiana. 

Cross  sections- for  Dane  county,  both  north  and  south,  and  east  and  west,  are  given 
on  Plates  XXIV  and  XXV,  showing  both  the  surface  contour,  and  the  succession  and  rela- 
tions of  the  several  strata.  Two  other  sections  through  the  county,  drawn  on  a  larger 
scale,  will  be  found  attached  to  Plate  XIII  of  the  Atlas.  These  sections,  with  the  col- 
ored map,  render  unnecessary  any  further  general  descriptions. 

On  the  east  side  of  the  county  the  lower  or  Buff  portions  of  the  Trenton  shows  in  nu- 
merous quarries,  many  of  which  yield  a  good  building  stone.  •  Amongst  many  quarries 
we  may  list  the  following:  N.  E.  qr.  Sec,  25,  York;  N.  E.  qr.  Seo.  26,  Medina,  a  large 
quarry  with  a  12  feet  face;  on  Sees.  29,  35  and  36,  Decrfield;  N .  E.  qr.  Sec.  22,  N.  E. 
qr.  Sec.  24,  and  N.  E.  qr.  Sec.  23,  Christiana,  the  last  one  showing  15  feet  of  regular, 
heavy  layers;  N.  W.  qr.  Sec.  2,  N.  E.  qr.  Sec.  15,  S.  W.  qr.  Sec.  £2,  N.  W.  qr.  Sec.  27, 
Albion;  S.  E.  qr.  Sec.  30,  Dunkirk,  where  there  is  a  15  feet  face;  S.  W.  corner  Sec,  3, 
N.  W.  qr.  Sec.  4,  N.  E.  qr.  Sec.  10,  where  there  are  10  feet  of  even,  heavy  layers,  S.  E. 
qr.  Sec.  13,  N.  E.  corner  Sec.  14,  N.  W.  qr.  Sec.  35,  S.  E.  qr.  Sec.  36,  Pleasant  Springs; 
Sec.  4,  Cottage  Grove;  N.  W.  qr.  Sec.  14,  N.  E.  qr.  Sec.  23,  Sun  Prairie;  N.  W.  qr. 
Sec.  17,  N.  E.  qr.  Sec.  30,  and  in  the  north  part  of  Sec.  34,  Bristol;  S.  E.  qr.  Sec.  14, 
N.  E.  qr.  Sec.  23,  Windsor;  S.  W.  qr.  Sec.  2,  S.  W.  qr.  Sec.  26,  N.  W.  qr.  Sec.  35, 
Burke;  N.  E.  qr.  Sec.  14  and  N.  E.  qr.  Sec.  11,  Windsor. 

The  quarry  on  the  N.  W.  qr.  Sec.  35,  Pleasant  Springs,  is  on  the  western  edge  of 
a  Trenton  area,  and  shows  15  feet  of  the  lowest  part  of  the  formation.  The  upper 
layers  are  thin,  whilst  the  lower  six  feet  are  taken  up  by  two  very  heavy  firm  layers, 
between  which  is  a  persistent  thin  seam.  2  inches  thick,  which  affords  large  regular 
paving  slabs.  The  limestone  is  yellowish,  much  marked  by  dendritic  oxide  of  man- 
ganese, and  is  easily  trimmed  into  smooth  blocks.  The  thin  upper  layers  show  numer- 
ous nests  of  crystals  of  limonite,  pseudomorphous  after  pyrite,  as  also  large  casts  of 
orthoceratites.  The  top  layer  is  glaciated,  the  striae  running  almost  due  south.  At  the 
bottom  of  the  quarry,  the  junction  with  the  St.  Peters  is  exposed.  A  wnll  near  by 
is  58  feet  in  the  latter  formation.  The  quarry  is  an  old  one,  having  been  opened  22 
years,  during  which  time  4,000  cords  of  stone  have  been  removed. 
The  quarry  in  the  north  part  of  Sec.  4,  Cottage  Grove,  shows  20  feet  of  tliin,  and 


•D 


I 


s  B 


THE  LOWER  SILURIAN  ROCKS.  601 

very  even-bedded,  close-textured,  yellowish,  limestone,  which  is  much  marked  by  dend- 
ritic manganese  oxide,  and  contains  the  following  fossils:  Petra'm  comic-iiluM,  Strophe- 
mena  alternate!,  a  small  Ortlils,  a  EhyiicoiieUa,  Cypricardifes  ventricosa,  Trodionona 
umbilicata,  Hclicotonta  planulata,  and  fragments  of  small  orthoceratites.  The  fossils 
are  casts  only. 

The  quarries  on  Sec.  23,  Sun  Prairie,  show  in  all  a  thickness  of  about  20  fec-t,  the 
upper  layers  of  which  are  thin,  shaly,  and  bluish  in  color,  and  appear  to  belong  to  th-3 
"Blue"  beds,  whilst  below  there  are  heavy  regular  layers  of  buff-colored  limestone. 
Immediately  beneath  the  shaly  layers  are  found  layers  of  a  very  close-textured,  purplish 
brown,  chonchoidal  fracturing  rock  (698),  carrying  Columnaria  alreolata.  From  the 
buff  layers,  the  following  fossils  were  obtained  (697,698):  Petra'm  cornicuJion,  Orthis 
trieenaria,  Strophomena  camemta,  Cypricardites  ventricosa,  very  large  casts  of  the  ex- 
terior of  Trochonema  umbilicata,  Eaphistotna  lenticularis,  a  Muchisonia,  Orthoceras 
rertebrale,  Orthoceras  anelhun,  Gyroccras  duplicostatum,  n.  sp.,  Oncoceras  pandion, 
and  cr'moidal  stems.  A  strong  lime,  hard  to  slack,  is  made  hero  from  the  buff  beds,  but 
the  stone  is  usod  chiefly  for  building  purposes. 

At  the  large  quarries  on  the  prairie,  in  the  north  half  of  Sec.  34,  Bristol,  are  exposed 
of  the  Blue  limestone  about  8  feet,  of  the  Buff  about  10  feet.  The  Blue  beds  show  a 
dark  bluish-gray  rock  (703).  with  a  flinty-textured  matrix,  in  which  are  scattered  numer- 
ous minute  strings  and  patches  of  calcite.  The  layers  of  this  rock  are  about  one-half  to 
there-fourths  inch  in  thickness,  very  rough-surfaced,  and  show  numerous  obscure  im- 
pressions of  fossils,  of  which  two  brachiopods,  Rhynconella  and  Strophornena,  appear  to 
be  most  abundant.  Between  these  layers  are  very  thin,  regular,  fragile,  dark  brown 
shaly  layers,  on  which  are  fine,  black,  graptolitc-like  markings.  The  rough-surfaced 
blue  layers  contain:  silica,  7.08;  alumina,  2.21;  carbonate  of  lime,  84.02;  carbonate  of 
magnesia,  5.33;  iron  peroxide,  0'83;  iron  protoxide,  0.39;  water,  0.61  =  100.42.  The 
Buff  beds  below  are  regular  heavy  layers  of  yellowish  close-textured  limestone,  includ- 
ing some  of  a  dark  purplish  brown,  chonchoidal-fracturing  rock,  like  that  already  men- 
tioned as  seen  on  Sec.  14  of  the  town  of  Sun  Prairie.  The  buff-colored  rock  (704),  from 
directly  below  the  junction  with  the  Blue,  contains:  silica,  4.45;  alumina,  &G8;  carbon- 
ate of  lime,  56.07;  carbonate  of  magnesia,  35.32;  iron  peroxide,  0.69;  iron  protoxide, 
0.58;  water,  0.46  —  99i65.  The  usual  fossil  casts  are  found  in  the  Buff  beds,  including 
fine  ones  of  Cypricardites  ventricosa  and  Gyrocems  duplicostatum. 

Fig.  50. 


[;/j:^;y!77^'.i--^ i - -: . ; ;\^vj /;'V-. : :J- .'•- --'--.-•:••.• :'.  ;'•'-. ^f^^^^^^^^{^^^<--:^^:~-y~-'l  :.'•'-"— ^\££&-. 
SECTION  ON  A  LINE  RUNNING  N.  25=  E.,  FROM  THE  S.  W.  QB.  OF  THE  S.  W.  QR.  OF  SEC.  2,  NEARLY 

TO  THE  NOKTH  LlNE  OF  SEC.  O,  JJURKK. 

Horizontal  scale  4  inches,  1  mile ;  vortical  scale  1  inch,  20D  feet. 

Fig.  50  represents  a  section  obtained  in  the  northern  part  of  the  town  of  Burke, 
showing  the  small  thickness  reached  by  the  St.  Peters  and  Lower  Magnesian  in  this 
part  of  the  county. 

In  the  small  quarry  on  the  N.  W.  qr.  Sec.  35,  in  the  same  town,  a  2  inch  layer  is 
crowded  with  impressions  of  the  exterior,  and  casts  of  the  interior,  of  the  following  fos- 
sils (694):  Petraia  Corniculum,  StropJwmena  camerata,  S.  incrassata,  Steptorhynchus 


C02  GEOLOGY  OF  CENTRAL  WISCONSIN. 

flitexta,  'S.  cleflecfa,  Oiihis  tricenaria,  Rhynconella,  n.  sp.,  Cypricardites  ventricosa, 
Raphistoma  lenticularis,  Pleurotomaria  siibconica,  Trochonema  umbilicata,  Murchisonia 
bicincta,  M.  tricarinata,  Orthoceras  anellitm,  0.  vertebrate. 

In  the  Catfish  Valley,  the  Potsdam,  Mendota,  Madison  and  Lower  Magnesian  are 
frequently  exposed,  the  last  three  being  quarried  at  numerous  places.  A  few  important 
points  only  can  be  mentioned.  O'Malley's  and  Veerhusen's  quarries  in  Westport  yield 
very  handsome  stone,  and  one  quite  different  from  the  general  run  of  the  Lower  Mag- 
nesian. O'Malley's  quarry,  S.  E.  qr.  S.  E.  qr.  Sec.  10,  shows  the  following  section: 

Ft.    In. 

1.  Thin  bedded  to  shaly  yellow  limestone 6     . . 

2.  Three  heavier  layers  of  the  same 2      6 

3.  Broken  yellow  limestone  with  much  oolitic  chert  (641)  and  geodic  calcite 

(642) 4     .. 

4.  Very  heavy  layers — inters tratified  with  two  or  three  thin  layers  —  of  cream- 

colored,  close,  granular-textured  Limestone  (640;,  containing  4.06  per 
cent,  of  argillaceous  impurities 10 

From  the  heavy  layers  of  No.  4,  one  of  which  has  a  thickness  of  24  inches,  some  2,000 
to  3,000  cords  have  been  removed,  the  stone  having  been  chiefly  used  in  the  construction 
of  the  State  Hospital  for  the  Insane.  Mr.  Veerhusen's  quarry,  N.  E.  qr.  of  the  S.  W. 
qr.  Sec.  25,  is  on  the  top  of  a  narrow  ridge  of  Lower  Magnesian,  and  has  a  face  of  24 
feet,  a  large  amount  of  stone  having  been  removed.  The  following  is  the  section,  be- 
ginning above: 

Ft.   In. 

1.  Rough,  brecciated,  yellow,  fine-granular  limestone  (629),  containing  3.49 

per  cent,  of  insoluble  ingredients;  bedding  indistinct 8 

2.  Very  heavy  layers,  some  4-5  feet  in  thickness,  of  pale  yellow,  close-textured, 

granular  limestone  (626,  627,  628),  which  on  solution  leaves  a  large  res- 
idue of  fine  gray  sand,  several  determinations  on  specimens  from  dif- 
ferent parts  of  the  face  giving  12.14, 13.03,  20.59, 34.74, 35.63,  and  40.78 
per  cents. ;  quarry  layers 15 

3.  Greenish  sandy  layer  (629)^);  a  specimen  on  solution  left  41.17  per  cent. 

of  very  fine  gray  sand 1 

4.  Thinner-bedded  limestone,  like  No.  2,  but  finer-grained,  of  greenish  tint, 

and  profusely  marked  with  dendritic  oxide  of  manganese;  below  the 

base  of  the  main  quarry;  thickness 8      6 

The  lowest  layer  is  39  feet  above  the  base  of  the  formation.  No.  2  lias  yielded  a 
very  large  amount  of  stone  for  the  construction  of  the  Insane  Asylum.  The  stone  is 
like  that  from  O'Malley's  quarry  on  Sec.  10,  and  should  have  much  wider  use  than  form- 
erly. It  is  a  much  handsomer  stone,  and  endures  weathering  better  than  the  sandstone 
used  in  Madison.  The  upper  and  less  sandy  layers  at  Veerhusen's  have  been  burned 
into  a  good  lime.  At  Westport  Station,  near  the  center  of  Sec.  26,  is  a  long  railroad 
cutting  through  the  western  end  of  the  ridge  upon  which  the  quarry  just  described  is 

situated.    The  deepest  part  of  the  cut  shows  the  following  section : 

Ft.    In. 

1.  Lower  Magnesian  limestone  (636);  gray-and-yellow-mottled,  porous,  mode- 

rately thin-bedded,  the  layers  somewhat  broken  and  displaced;  con- 
tains 11.52  percent,  of  argillaceous  impurities;  at  base  is  a  thin  layer  of 
white  oolitic  chert,  and  another  of  greensand;  in  all 20 

2.  Madison  sandstone,  including:  thick-bedded,  yellowish,  fine-grained  sand- 

stone (637),  with  only  2  per  cent,  of  soluble  ingredients,  19  feet;  lighter 
colored  sandstone,  2  feet  6  inches;  and  purely  silicious,  white  sandstone, 
4    often  loose,  and  composed  of  much  rolled  quartz  grains,  4  feet;  in  all. .     25      6 


THE  LOWER  SILURIAN  ROCKS.  603 

The  quarry  on  the  north  side  of  the  marsh,  in  the  X.  W.  qr.  of  Sec.  12,  Springfield. 
is  on  the  Madison  sandstone,  whose  upper  layers  here  are  heavy,  regular,  buff-colored, 
contain  over  40  per  cent,  of  soluble  ingredients,  and  make  a  good  building  stone,  re- 
sembling that  quarried  at  the  same  horizon  nea-r  Madison.  Heiny's  quarries,  on  the 
Lower  Magnesian,  N.  W.  qr.  Sec.  35,  Springfield,  are  quite  extensive.  They  show  the 
following  section: 

Feet. 
\.  Concretionary  and  brecciated  yellow  limestone 5 

2.  Heavily-bedded  white  layers  with  riiuch  chert,  burnt  for  lime ...     10 

3.  Xo  exposure 25 

4.  Irregularly  thin-bedded,  porous,  white-and-yellow-mottled  limestone  (648),  with 

geodic  cavities,  many  black  dendritic  markings,  and  6.11  per  cent,  of  insoluble 
ingredients 15 

The  lowest  exposure  is  near  the  base  of  the  formation. 

The  Madison  sandstone  and  overlying  Lower  Magnesian  are  finely  exposed  in  a  large 
quarry  on  the  edge  of  the  high  land,  S.  E.  qr.  Sec.  11,  Midtlleton.  The  following 
section,  taken  here,  is  interesting  as  showing  how  the  great  Lower  sandstone  series 
graduates  upward  into  the  Lower  Magnesian;  the  order  is  as  usual  a  descending  one: 

LOWER  MAGNESIAN. 

Ft.    In. 

1.  Very  irregular  layers,  alternatingly  thick  and  thin,  of  a  brownish-gray, 

close-textured,  minutely -crystalline,  chcrty  limestone  (591),  which  leaves 
on  solution  4.39  per  cent,  of  a  very  fine,  clayey  residue;  7  feet  below  the 
top  is  a  marked  concretionary  layer,  one  foot  thick 18  4 

2.  Brecciated  lay-er  of  sandy,  grayish  Limestone  (592),  containing  63.89  per 

cent,  of  fine  gray  quartz  sand 1 

3.  Thick  layer  of  gray,  flinty- textured  limestone,  with  a  thin,  sandy  layer  at  top      1      1 

4.  Concretionary,  cavity- bearing  limestone  (593),  which  leaves  on  solution 

11.03  per  cent,  of  fine,  grayish,  aluminous  residue;  the  cavities  carry  dol- 
omite crystals 4  4 

5.  Yellowish  calcareous-sandstone 10 

6.  Yellowish  limestone,  in  places  quite  sandy 2     . . 

7.  Very  close-textured,  non-crystalline,  yellowish  limestone  (594),  containing 

9.19  per  cent,  of  fine,  aluminous,  insoluble  matter,  and  much  marked  by 
dendritic  oxide  of  manganese 2  2 

8.  Brownish,  sandy,  porous  limestone  (59o,  652),  carrying'  oolitic  chert,  numer- 

ous crystal-lined  cavities,  and  containing  28.04  per  cent,  of  sand 2      2 

9.  Yellow-and-gray-mottled,  rough-textured,  conchoidal- fracturing  limestone 

(596),  containing  3.89  per  cent,  of  aluminous  impurities 1 

10.  Oolitic  chert  layer  (597;  nearly  pure  quartz,  only  .01  per  cent,  being  solu- 

ble        6 

MADISON    BEDS. 

11.  Pure  white,  exceedingly  fine  sandstone  (598,  651),  composed  of  angular  tc 

rolled  grains  of  translucent  quartz;  often  loose  sand;  the  layer  very  ir- 
regular, swelling  down  and  cutting  oft' the  layers  below;  in  some  places 
cutting  oft'  also  the  layers  above ;  tlu'ckness  varies  from  7  inches  to 1  5 

12.  Light  yellow,  friable,  fine-grained,  dolomitic  sandstone  (599,  650),  composed 

of  rolled  quartz  grains  embedded  in  a  crystalline  dolomitic  matrix;  the 
sand  being  63.4  per  cent,  of  the  rock;  the  exact  equivalents  of  the  Mad- 
ison building- stone;  thickness 15  7 

Total 49      6 


604  GEOLOGY  OF  CENTRAL  WISCONSIN. 

The  following  is  the  section  at  MacBricle's  point,  on  the  north  shore  of  Lake  Mendo- 
ta,  N.  W.  qr.  Sec.  1,  Madison: 

I.  Heavy-bedded,  jointed  Mendota  limestone  (684),  having  a  brown  color,  and 

close-grained,  flinty  matrix,  and  leaving  on  solution  15.05  per  cent,  of  a 
fine  sandy  residue;  layers  run  2  to  4  feet  in  thickness;  joints  N.  87°  W., 
used  in  construction  of  old  capitol  at  Madison 21  8 

II.  Thin- laminated  yreensand  layer 1 

III.  Upper  layers  of  fotsdam  sandstone;  fine-grained,  light-greenish-tinted, 

calcareous  sandstone,  containing  15.5  per  cent,  of  soluble  ingredients; 
thin-bedded,  alternate  layers,  different  colors;  some  more  calcareous 
layers  weathering  in  relief;  scolithus-bvaring 31 

On  the  N.  W.  qr.  Sec.  21,  and  the  N.  E.  qr.  Sec.  20,  Madison,  is  a  round  isolated  hill 
capped  by  the  Lower  Magnesian.  The  top  of  the  hill  is  almost  completely  encircled  by 
a  large  quarry  which  exposes  the  Lower  portions  of  the  Lower  Magnesian  and  the  upper 
part  of  the  Madison  sandstone.  The  following  section  includes  the  quarry  face  and  the 
record  of  a  well  near  by: 

LOWER   MAGXESIAN. 

Fl.    In. 

1.  Yellow,  fine,  granular,  close  textured    limestone    (607);  thin  bedded  to 

shaly;  some  few  layers  near  the  top  are  burnt  for  lime 5      8 

2.  Gray-and-yellow-mottled,  porous  limastone  (603,  611-),  with  large  patches 

of  rhombohedral  calcite,  much  dendritic  manganese  oxi:le,  and  4.1  per 
cent,  insoluble  matter;  forming  one  layer 2 

3.  Thin-bedded  to  shaly  yellow  limestone,  mostly  quite  sandy 10 

4.  Layer  burnt  for  lime  (606)  and  containing  only  2.3  per  cent,  of  insoluble 

ingredients , 8 

5.  Layer  of  oolitic  chert  (608);  a  milk-  white  material  made  up  of  little  con- 

eretions  -fa  to  TV  inch  in  diameter,  which  consist  of  minute  rounded  grains 
of  limpid  quartz  encased  in  a  milk- white  powdery  matrix;  having  the  fol- 
lowing composition :  silica,  98.01;  alumina,  0.53;  iron  sesquioxide,  0.73; 

lime,  0.67;  magnesia,  0,21=100.1i>;  thickness,  one  inch  to 6 

MADISON. 

6.  Greensand  layer,  consisting  of  a  matrix  of  rounded  quartz- grains  and  dark 

green  grains  of  glauconite  . , 1      6 

7.  Light  buff-colored  sandstone  (604);  in  heavy  uniform  layers  six  inches  to 

two  feet  in  thickness;  much  used  as  a  building  stone  in  Madison:  con- 
tains 10  per  cent,  of  carbonates  of  lime  and  magnesia 12 

8.  Light-colored  sandstone,  similar  to  the  foregoing  but  less  firm  and  regular; 

in  the  lowest  portions  at  the  base  of  the  quarry  a  loose  white  sand ...       5      8 

9.  Unexposed,  below  the  quarry  base 5 

10.  Soft  red  and  brown  sandstone  in  well 14     . . 

MEXDOTA. 

11.  Hard  yellow  limestone,  in  well 30 

POTSDAM. 
12  Soft  greenish  sandstone,  in  weh1 20 

107     .. 

The  building  stone  of  these  quarries  is  much  sought  for.     It  is  obtained  also  from 
quarries  across  a  small  valley,  on  the  N.  W.  qr.,  Sec.  21.    It  was  formerly  worked  to  u, 


THE  LOWER  SILURIAN  ROCKS.  605 

considerable  extent  on  the  side  of  the  hill  on  sections  17  and  18,  and  beyond  doubt  is  to 
be  found  in  the  neighboring  country  at  many  other  fovorably  located  points.  This  is  a 
matter  of  some  importance,  since  in  the  present  quanies  the  stripping  has  become  a 
heavy  expense. 

At  Madison,  the  Mendota  is  exposed  in  several  small  railroad  cuttings  (622)  on  the 
north  side  of  Sec.  22.  On  the  S.  W.  qr.  Sec.  23,  on  the  point  of  a  low  ridge  projecting  into 
the  marsh,  is  a  quarry  of  some  size,  showing  the  lower  10  feet  of  the  Mendota  limestone. 
The  upper  layers,  are  thin,  the  lower  heavier,  and  all  very  irregular.  The  rock  (613)  is 
a  dark  yellow  to  brownish,  rough- textured,  concretionary  limestone,  containing  many 
red  patches  of  iron  oxide,  which  proceeds,  apparently,  from  the  oxidation  of  pyrite.  The 
composition  is:  silica,  4.18;  alumina,  2.17;  iron  peroxide,  1.45;  carbonate  of  lime,  55.68; 
carbonate  of  magnesia,  35.52;  water,  0.58=100.58.  Greensand  in  scattering  grains,  and 
light  green  earthy  patches  are  seen  throughout,  whilst  a  regular  greensancl  layer  (612) 
at  the  bottom  of  the  quarry  marks  the  base  of  the  formation.  Towards  the  side  of  the 
ridge  the  limestone  layers  have  an  inclined  position  due  to  undermining.  This  quarry 
was  one  of  the  first  points  at  which  the  Mendota  was  recognized,  and  may  be  regardeu 
as  typical  of  the  lower  part  of  the  formation.  The  rock  has  many  points  in  common 
with  the  Lower  Magnesian,  being  quite  as  free  from  sand  as  that  rock. 

The  Artesian-boring  in  the  Capitol  park  at  Madison  has  a  depth  of  1,015  feet,  pene- 
trating in  its  course  Glacial  Drift,  the  Potsdam  sandstone,  and  200  feet  of  the  Archaean 
rocks.  The  water  in  the  well  comes  within  some  60-70  feet  of  the  surface,  from  where 
it  is  pumped  for  use  in  the  boilers  at  the  Capitol  and  for  drinking  purposes.  It  is  re- 
garded as  a  "mineral  "  water,  but  is  not  one,  being  freer  from  solid  ingredients  than 
ordinary  well  water,  and  containing  nothing  unusual  except  a  small  quantity  of  iron 
bicarbonate,  the  iron  of  which,  on  exposure  to  the  air,  peroxidizes,  and  produces  a 
brownish  sediment.  A  record  of  this  boring  has  already  been  given  in  the  annual  re- 
port of  Dr.  Lapham,  page  50;  the  greenish  mineral  from  the  rock  at  the  bottom  of 
the  well  is,  however,  probably  not  prehnite,  as  there  given.  The  Artesian  boring  at  the 
Milwaukee  and  St.  Paul  depot  begins  at  a  level  74  feet  below  the  top  of  the  boring  in 
the  Capitol  park,  and  brings  water  to  within  7  feet  of  the  surface.  The  following  is 
an  abbreviated  register  of  this  boring : 

Feet. 

Drift:  sand  and  clay,  with  bowlders;  the  lower  part  nearly  all  loose  sand,  so  that 
it  is  difficult  to  tell  where  the  drift  ends  and  the  underlying  sandrock  be- 
gins ;  about 70 

Potsdam  sandstone:  specimens  from  depths  of  200,  250,  290,  350,  360,  380  and 
390  feet  show  very  fine,  white  quartz  sand,  stained  here  and  there  with 
deep  brown  points  of  iron  oxide,  and  entirely  non -calcareous;  some  of  the 
sand  is  a  little  coarser,  and  all  as  s?en  under  the  microscope  is  made  up  of 
very  much  rolled  grains,  the  larger  ones  of  which  are  almost  wholly  spher- 
ical. Specimens  from  600  and  680  feet  are  also  of  limpid  quartz,  but  the 
grains  are  very  much  coarser  and  less  rounded.  The  lowest  layer  of  the 
formation  struck  is  soft  red  shale,  like  that  found  in  the  Capitol  well. 

Thickness  in  all,  about 665 

Arclwean :  dark  colored  rock,  like  that  in  'the  Capitol  well   50 

Depth  of  boring 785 

The  lower  layers  of  the  Madison  sandstone  are  quarried  on  the  S.  E.  qr.  Sec.  28, 
Madison,  on  the  south  shore  of  Lake  Wingra,  and  the  same  rock  is  finely  exposed  (614, 
617)  with  a  thickness  of  23  feet,  largely  pure  white  sand,  and  overlaid  by  17  feet  of  non- 
arenaceous  thin-bedded  Lower  Magnesian,  in  the  railroad  cutting,  S.  E.  qr.  Sec.  35. 
About  35  feet  below  the  bottom  of  this  cut,  10  feet  of  Mendota  'is  exposed  on  the 


600  GEOLOGY  OF  CENTRAL  WISCONSIN. 

south  shore  of  Lake  Monona,  near  the  S.  E.  corner  of  Sec.  26.     On  the  south  line  of  the 
town  of  Madison,  Sec.  33,  a  large  quarry  on  the  Lower  Magnesian  shows  the  following1, 

beginning  above : 

Ft.    In. 

1.  Concretionary  and  irregularly  bedded,  yellowish-gray  limestone 10 

2.  Chert  layer;  sometimes  forming  a  continuous  nodular- surfaced  layer,  at 

others  occurring  in  a  row  of  separate  nodules;  internally,  the  chert 
(644)  is  brown-and-white-banded,  and  jaspery;  externally  it  has  a  soft, 
white,  silicious  coating 3 

3.  Compact,  heavily  bedded,  flinty-textured,  gray  limestone  (644)  containing  a 

few  geodic  cavities  lined  with  dolomitic  crystals;  composed  of  silica, 
1.09;  alumina,  0.44;  iron  peroxide,  0.43;  iron  protoxide,  0.63;  lime 
carbonate,  66.82;  magnesia  carbonate,  30.40;  water,  0.35=100.16;  thick- 
ness    4 

4.  Chert  layer,  like  No.  2 2 

5.  Very  heavily  bedded  limestone,  like  No.  1 5 

Throughout  the  quarry  there  is  a  marked  local  dip  of  10°  to  15°  southward.  The 
quarries  have  been  opened  for  20  years,  the  etone  being  used  altogether  for  burning  into 
lime,  of  which  about  20,000  bushels  are  made  annually  in  two  large  kilns. 

On  the  west  shore  of  Lake  Kegonsa,  near  the  center  of  Sec.  26,  Dunn,  a  large  ex- 
posure shows  the  following: 

Fed. 

I.  White  sandstone  with  brownish  stains 1 

II.  Greensand  layer 2 

III.  Light-colored,  soft,  thin-bedded,  calcareous  sandy  layers,  with  specks  of  green- 

sand  and  geodic  calcite 1 

IV.  Whitish  layer,  more  calcareous  than  the  preceding ...       2 

V.  Heavily-bedded,  light  yellowish  sandstone  (693);   fine-grained,  firm,  nearly 

one-half  soluble,  the  residue  made  up  of  angular  to  subangular  white  sand; 

in  parts  cross-laminated 12 

VI.  Sandy,  yellowish,  fine-grained  limestone 12 

30 

The  lowest  layers  are  unmistakably  Mendota,  which  is  here  much  less  sharply  defined 
than  usual  from  the  Madison.  One-half  mile  north,  friable,  brownish,  entirely  non- 
calcareous,  Madison  sandstone  is  seen  on  the  hill  side,  corresponding  to  the  uppermost 
layers  of  the  foregoing  section.  A  similar  sandrock  shows  near  the  roadside  on  the 
north  line  of  the  N.  W.  qr.  of  Sec.  27,  at  the  Town  House,  on  the  center  of  the  south 
line  of  Sec.  21,  and  in  the  field  near  the  middle  of  the  S.  E.  qr.  Sec.  21,  the  last  named 
lying  near  to,  and  about  15  feet  below,  one  of  Lower  Magnesian.  All  of  these  exposures 
appear  to  carry  the  Madison  to  an  unusual  thickness,  50  or  60  feet, 

On  the  divide  Itetweem  the  Catfish  and  Sugar  river  valleys,  in  Middleton,  Verona, 
Fitchburg,  Montrose  and  Oregon,  the  Trenton  is  the  rock  most  commonly  quarried,  be- 
ing obtained  from  the  tops  of  isolated  ridges  whose  sides  often  show  large  exposures  of 
the  St.  Peters.  Amongst  other  quarries  may  be  named  those  on  the  S.  E.  qr.  Sec.  27 
(662,  663,  669),  and  the  S.  E.  qr.  Sec.  35  (664,  665,  666),  Middleton;  the  very  large 
quarries  on  Sees.  7,  15  and  18,  Fitchburg;  those  on  Sees.  13  and  26,  Montrose;  those  on 
Sees.  4  and  24,  Oregon;  and  those  on  Sees.  28  and  35,  Rutland.  All  of  these  are  in  the 
Buff  beds,  generally  close  to  the  St.  Peters. 

In  the  Sugar  river  valley  and  its  branch  valleys  the  Trenton  is  quarried  at  a  few 
points,  but  the  St.  Peters  makes  very  frequent  natural  exposures  of  large  size.  ClifS? 


THE  LOWER  SILURIAN  ROCKS.  607 

and  shelving  ledges  of  brownish,  friable  St.  Peter's  are  frequent  on  the  valley  sides,  and 
isolated  bluffs  and  towers  of  the  same  rock  are  to  be  seen  at  several  places  within  the 
valleys  themselves.  One  of  these  towers,  on  the  S.  W.  qr.  of  the  S.  E.  qr.  Sec.  11 
Primrose,  known  as  the  Devil's  Chimney,  is  circular  in  section,  60  feet  high,  50  feet  in 
diameter  on  the  top  and  40  feet  at  the  bottom.  The  isolated  bluff  on  the  N.  E.  qr.  of 
the  S.  W.  qr.  of  Sec.  28,  Springdale,  is  100  feet  high,  100  yards  in  diameter  at  base  and 
20  on  top. 

On  tlie  Wisconsin  river  slope  the  exposures  and  quarries,  which  are  numerous,  are 
chiefly  in  the  Potsdam,  Mendota,  Madison  and  Lower  Magnesian.  The  Trenton  is 
quarried,  however,  on  the  N.  E.  qr.  of  Sec.  18,  Middleton,  at  the  top  of  a  high  bluff, 
showing  90  feet  of  St.  Peters  (658)  as  represented  in  Fig.  51. 

FIG.  51. 


SECTION  ACROSS  THE  VALLEY  OP  BLACK  EARTH  CREEK. 
Vertical  scale  200  feet  to  the  inch.    Horizontal  scale  400  feet  to  the  inch. 

The  Trenton  at  this  place  (659,  660,  661)  contains  numerous  casts  of  the  following 
fossils:  Pet raia  corniculum,  Strophomena,  Cypricarditesventricos:isRapliistomalenticu- 
lare,  Trochonema  umbilicata,  Murchisonia  bicincta,  M.  tricarinata,  Pleurotomaria  Nz- 
soni,  Oncoceras  pandion,  and  Orthoceras  anellum.  The  Trenton  shows  also  in  a  small 
quarry  at  the  top  of  the  bluff  on  the  N.  W .  qr.  of  Sec.  28,  Beiry,  far  away  from  any 
other  Trenton  area. 


COS  GEOLOGY  OF  CENTRAL  WISCONSIN. 


CHAPTEE  V. 
THE    QUATERNARY   DEPOSITS. 

THE  GLACIAL  DRIFT.1 

The  first  and  most  striking  fact  that  presents  itself  to  the  investi- 
gator of  the  drift  phenomena  of  Wisconsin  is  the  existence  of  an 
extensive  driftless  region,  the  remainder  of  the  state  at  the  same 
time  displaying  an  altogether  extraordinary  development  of  the  drift 
materials.  In  the  driftless  region,  which  occupies  12,000  square 
miles  of  the  southwestern  part  of  Wisconsin,  or  nearly  one-fourth 
the  entire  area  of  the  state,  the  drift  is  not  merely  insignificant,  but 
absolutely  wanting.  Except  in  the  valleys  of  the  largest  streams, 
like  the  Wisconsin  and  Mississippi,  not  a  single  erratic  bowlder,  nor 
even  a  rounded  stone,  is  to  be  seen  throughout  the  district;  whilst  the 
exception  named  is  not  really  an  exception,  the  small  gravel  deposits 
that  occur  on  these  streams  having  evidently  been  brought  by  the 
rivers  themselves,  during  their  former  greatly  expanded  condition, 
from  those  portions  of  their  courses  that  lie  within  the  drift-bearing 
regions. 

The  outline  of  the  driftless  area  is  for  the  most  part  quite 
sharply  defined,  both  by  a  more  or  less  sudden  cessation  of  the  drift 
materials,  and  by  a  change  in  the  topography  as  the  line  is  crossed 
from  one  side  to  the  other.  This  is  more  especially  true  of  the  east- 
ern boundary,  close  to  which  are  often  found  heavy  morainic  heaps, 
with  numerous  bowlders  of  a  large  size,  and  on  the  different  sides  of 
which  the  topographical  effects  of  purely  subaerial  erosion  with- 
out drift,  and  those  of  partial  glacial  erosion  with  drift,  are  strongly 
contrasted.  The  northern  boundary,  on  the  contrary,  is  largely  in  a 
level  country,  the  drift  materials  increasing  quite  gradually  in  quan- 
tity as  it  is  left  behind  to  the  southward. 

1  It  is  not  possible  to  give,  in  the  space  available,  more  than  a  brief  summary  of  the 
large  amount  of  material  with  regard  to  the  glacial  drift  that  has  been  obtained  during 
the  survey  of  the  Central  Wisconsin  district,  with  the  main  conclusions  reached. 
These,  it  is  believed,  when  taken  together  with  the  results  of  the  work  of  6ther  mem- 
bers of  the  corps,  will  be  found  of  considerable  interest. 


MAP    OF   PART   OF    WISCONSIN 

dfsignfcl  tc  .ihcu'  the  mtiiii  /iirf*   tritli  regard  to  the  distribution  cf  fiir 

G  LA  C  I AL,  DRIFT 

find  of  her- 

:  ATK  R  >:AI?>'  D  E  T»  o  s  IT  s .        PLAT  £  XXVA . 

" 


[  I  ;  i  i  f.  *  •  »• 

a.  Jfri/ibfarinff^rra    Lacustrine  f/a\y         Aforaiiiic  Drift       Small  LakesMitlwi  it  outlet 

GlofialStriat  (  KttOerungf  ) CcnntyUn, 

Drift  limit  and,m0raine,sonth  pfTown  .^.  after  Moses  Strong  and  T.C.Chantberiai 


THE  GLACIAL  DRIFT.  609 

Plate  XXVI  shows  the  boundary  of  the  driftless  region  for  the  lar- 
ger part  of  its  extent  in  Wisconsin.  This  line  lies  chiefly  in  the  Cen- 
tral Wisconsin  district,  but  for  the  four  townships  south  of  Dane 
county  has  been  copied  from  the  maps  of  Mr.  Strong.  Entering 
Dane  county  on  the  middle  of  the  south  line  of  Montrosej  T.  5,  R.  8 
E.,  it  nearly  coincides  with  Sugar  river  as  far  as  the  head  of  that 
stream  in  Cross  Plains,  T.  7,  R.  7  E.  Along  this  portion  of  its 
course  the  heaviest  drift  deposits  are  several  miles  to  the  eastward  of 
the  boundary,  which  they  gradually  near  to  the  northward.  From 
the  head  of  Sugar  river  the  divide  is  crossed  to  Black  Earth  river,  the 
northern  side  of  which  is  followed  into  the  towns  of  Black  Earth  and 
Mazomanie,  T.  8,  R.  6  E.  Thence,  bending  northward,  and  cross- 
ing the  Wisconsin  between  Sank  City  and  the  mouth  of  Honey  creek, 
the  line  pursues  a  northerly  course  across  Sauk  Prairie  to  the  foot  of 
the  Baraboo  quartzite  ranges,  morainic  drift  occurring  from  half  a 
mile  to  two  or  three  miles  east  of  it.  On  top  of  the  quartzite  ranges 
no  drift  is  seen  west  of  Devil's  Lake,  in  whose  valley  are,  however, 
heavy  deposits,  and  the  line  appears  thus  to  make  a  slight  bend  east- 
ward. North  of  the  ridge,  however,  it  is  further  west  again,  for  large 
heaps  occur  at  Baraboo,  and  bowlders  are  to  be  seen  two  or  three 
miles  west  of  that  place. 

Beyond  the  Baraboo,  the  line  continues  in  a  northerly  direction  to 
the  north  line  of  Sauk  county,  where  it  bends  out  to  the  westward 
along  the  high  ground  that  forms  the  rim  of  the  sand  plain  of  Juneau 
and  Adams  counties,  for  granitic  and  other  bowlders  may  be  seen 
all  along  the  road  from  Kilbourn  to  Mauston,  as  far  as  the  N".  W.  qr. 
of  Sec.  27,  T.  14,  E,.  5  E.  Very  soon,  however,  a  sharp  bend  is  made 
to  the  eastward  again,  the  line  following  the  inner  edge  of  the  high 
ground  to  the  Wisconsin,  above  the  Dalles,  and,  after  crossing  the 
river,  in  a  curving  direction  through  southeastern  Adams  county. 
Turnino-  then  northward,  it  lies  a  short  distance  west  of  the  east  line 

O  ' 

of  that  county,  until  its  northern  portion  is  reached,  when,  curving 
once  more  to  the  westward,  it  crosses  the  Wisconsin  again  near 
Grand  Rapids,  in  Wood  county.  A  sketch  map  of  the  Wisconsin 
driftless  area,  given  by  J.  D.  Whitney, 1  includes  all  of  Adams  and 
the  eastern  part  of  Juneau  counties  within  the  drift-bearing  area, 
and  shows  the  limit  altogether  to  the  west  of  the  Wisconsin.  This 
portion  of  the  state  he  does  not,  however,  seem  to  have  mapped  from 
personal  investigation.  I  have  never  seen  any  sign  of  glacial  drift  in 
the  district  specified,  and,  indeed,  the  numerous  fragile  sandstone 
peaks  occurring  within  it  preclude  the  idea  that  the  glacial  forces 

1  Geological  Survej  of  Wisconsin,  Vol.  I.    Albany,  1862. 
Wis.  SUB.— 39 


CIO  GEOLOGY  OF  CENTRAL  WISCONSIN. 

could  ever  have  acted  there.  Flanking  the  north  side  of  the  quartz  - 
ite  bluff  at  J^ecedah,  in  Juneau  county,  is  a  great  bank  of  gravel  and 
rounded  bowlders,  but  these  are  wholly  of  quartzite,  derived  from  the 
bluff  itself,  and  must  hence  be  regarded  as  the  result  of  river  or  lake 
action  upon  the  quartzite.  Clay  and  sand  deposits  occur  in  much  of 
Adams  county,  as,  for  instance,  around  Friendship,  but  are  finely  lam- 
inated, and  appear  to  be  due  to  deposition  from  expanded  streams  or 
lakes,  being  wholly  without  associated  gravel.  From  southern  to 
northern  Adams,  the  drift  limit,  as  marked  by  the  loose  materials  of 
the  surface,  is  for  the  most  part  directly  along  the  edge  of  heavy  mo- 
rainic  heaps,  with  numerous  bowlders. 

Westward  from  Grand  Rapids,  the  drift  limit  is  not  always  so  well 
defined,  but  does  not  appear  to  be  far  from  the  line  of  the  Green  Bay 
and  Minnesota  railroad,  as  far  as  the  crossing  of  Black  river.  From 
here  it  bends  to  the  northeast,  crossing  the  line  of  the  West  Wiscon- 
sin road  some  twelve  miles  southeast  of  Eau  Claire. 

The  nature  of  the  topography  of  the  driftless  area,  everywhere 
most  patently  the  result  of  subaerial  erosion  exclusively,  is  even  more 
striking  proof  that  it  has  never  been  invaded  by  the  glacial  forces 
than  is  the  absence  of  the  drift  material.  Except  in  the  level  country 
of  Adams,  Juneau,  and  eastern  Jackson  counties,  it  is  everywhere  a 
region  of  narrow,  ramifying  valleys,  and  narrow,  steep-sided,  dividing 
ridges,  whose  directions  are  towards  every  point  of  the  compass,  and 
whose  perfectly  coinciding  horizontal  strata  prove  conclusively  their 
erosive  origin.  A  glance  at  the  map  of  Plate  XXVI,  on  which  are 
accurately  represented  all  but  the  very  smallest  streams,  will  serve  to 
give  an  idea  of  this  feature  of  the  driftless  area.  Each  one  of  the 
numerous  streams  shown  has  its  own  ravine,  and  the  ravines  are  all 
in  direct  proportion  to  the  relative  sizes  of  the  streams  in  them.  This 
is  well  brought  out  by  the  colored  geological  maps  of  Areas  D,  E,  G 
and  H,  in  the  Atlas.  Since  the  several  strata  lie  nearly  horizontal, 
the  colors  representing  them  give  really  a  close  idea  of  the  topography. 
The  two  first  named  maps  include  portions  of  both  drift-bearing  and 
driftless  areas,  and  the  different  appearances  of  the  geological  outlines, 
stream  and  marsh  directions,  etc.,  on  the  east  and  west  sides  of  the 
maps,  are  very  instructive.  It  should  be  said  that  this  difference  is 
due,  also,  partly,  but  not  mainly,  to  a  change  which  takes  place  mid- 
way within  the  districts  represented  by  these  maps,  from  a  nearly 
perfect  east  and  west  horizontal! ty  of  the  strata  to  a  small,  but  grad- 
ually increasing,  eastward  descent.  In  this  connection,  reference 
should  also  be  made  to  Mr.  Strong's  excellent  contour  maps  of  the 
lead  region. 


THE  GLACIAL  DRIFT.  611 

In  the  central  plain  of  Adams  and  Juneau  counties,  though  the 
ramifying  ridge-and- valley  topography  is  wanting,  no  less  indisputa- 
ble topographical  proof  is  at  hand  of  the  immunity  of  the  region  from 
the  glacial  action  in  past  time;  for,  dotting  the  surface  of  the  plain, 
we  find  the  numerous  sandstone  towers  that  have  been  so  often  alluded 
to  in.  this  report.  The  fragile  character  of  these  peaks  is  sufficient 
evidence  that  they  could  never  have  stood  in  the  path  of  a  glacier. 

The  altitude  of  the  driftless  area,  as  compared  with  the  drift- 
bearing  regions,  becomes  a  matter  of  some  importance  in  any  attempt 
to  explain  the  absence  of  the  drift  phenomena.  It  has  been  stated 
by  some  writers  that  the  driftless  area  is  higher  than  the  drift-bearing, 
and  was,  consequently,  not  subjected  to  glacial  invasion.  It  is  true 
that  in  general  the  eastern  half  of  the  state  ie>  lower  than  the  western, 
but  from  what  follows  it  will  be  seen  that  farther  than  this  the  state- 
ment is  inaccurate.  From  the  south  line  of  the  state  as  far  north  as 
the  head  of  Sugar  river,  in  Cross  Plains,  the  country  west  of  the  drift 
limit  rises  rapidly  200-400  feet.  Just  north  of  the  head  of  Sugar 
river,  the  limit  crosses  high  ground  —  the  western  extension  of  the 
high  limestone  and  prairie  belt  of  northern  Dane  and  southern  Colum- 
bia counties  —  and  the  altitudes  east  of  the  limit  are  as  great  as  those 
to  the  west;  whilst  in  passing  from  the  head  of  the  Catfish  river  west- 
ward, a  glacier  must  have  made  an  abrupt  ascent  of  fully  300  feet. 
North  of  Black  Earth  river,  the  limit  has  the  higher  ground,  by  200 
feet,  on  the  east.  Sank  prairie  is  crossed  on  a  level,  and  though 
higher  ground  occurs  west  of  the  prairie,  its  topography  and  the  ab- 
sence of  drift  show  that  the  glacier  never  reached  so  far.  "Where  the 
quartzite  range  north  of  Sank  Prairie  is  crossed  by  the  limit,  it  is 
higher  (850  feet  above  Lake  Michigan)  than  any  part  of  the  driftless 
area  except  the  Blue  Mounds,  whilst  a  few  miles  east  a  great  develop- 
ment of  bowlders  and  gravel  is  found  on  one  of  the  highest  portions 
of  the  range  (900  to  950  feet  altitude).  From  the  Baraboo  north  to 
the  Sauk  county  line,  there  appears  to  be  no  relation  between  the 
position  of  the  limit  and  the  altitude  of  the  country.  From  the  north 
line  of  Sauk  county,  in  curving,  as  previously  described,  to  the  east- 
ward and  northward  around  Adams  county,  the  limit  is  on  the  very 
crest  of  the  divide.  From  its  position  near  the  middle  of  the  east 
line  of  Adams  county,  the  country,  for  40  miles  to  the  west,  is  from 
100  to  200  feet  lower.  From  the  northwest  part  of  Adams  county 
to  the  "Wisconsin  river  the  limit  is  in  a  level  coantry ;  whilst  from  the 
Wisconsin  westward  the  country  north  of  it  is  everywhere  much 
higher  than  that  to  the  south,  the  rise  northward  continuing  to  within 
thirty  miles  of  Lake  Superior. 


612  GEOLOGY  OF  CENTRAL  WISCONSIN. 

The  surface  features  of  the  drift-bearing  regions,  so  far  as  they 
are  independendent  of  the  rocky  formations  beneath,  are  in  strong 
contrast  with  those  of  the  driftless  area.  There  is  an  almost  entire 
absence  of  the  narrow  ridge- and -valley  topography,  or  of  very  steep- 
sided  valleys  generally,  the  contours  being  everywhere  more  flowing. 
The  difference  is  evidently  due  both  to  a  different  method  of  erosion 
and  to  the  obliteration  of  abrupt  changes  of  level  by  heavy  deposi- 
tions of  drift  materials  Another  marked  difference  is  noticed  in  the 
entire  absence,  east  of  the  drift  limit,  of  the  fragile  castellated  out- 
liers that  are  found  further  west.  Outliers  do  occur,  though  not 
abundantly,  but  are  thick  and  of  rounded  contour,  and  more  com- 
monly of  limestone.  Still  another  contrast  is  presented  in  the  linear, 
and  for  considerable  areas  parallel,  arrangement  of  the  ridge,  valley, 
marsh,  and  stream  directions,  and  also  of  the  outlines  of  the  areas  oc- 
cupied by  the  several  formations,  as  compared  with  the  ramifying 
arrangement  of  the  driftless  region.  To  these  features  of  the  drift- 
bearing  districts  are  to  be  added  the  peculiar  appearance  due  to  round- 
ed hills  and  winding  ridges  of  pebbles  and  sand,  the  abundance  of 
circular  and  serpentine  depressions  without  outlet,  and  often  occupied 
by  lakes  of  considerable  size,  and  the  omnipresent  surface  erratics  — 
all  of  which  receive  especial  attention  below. 

The  features  thus  enumerated  are  especially  to  be  observed  in  that 
part  of  the  state  which  lies  east  of  the  eastern  boundary  of  the  drift- 
less  area,  the  region  lying  immediately  north  of  its  northern  bound- 
ary, though  showing  in  parts  considerable  quantities  of  drift  material, 
having  apparently  not  been  subjected  to  so  great  glaciation.  In  much 
of  the  latter  region  the  drift  appears  to  be  quite  insignificant,  and  all 
surface  irregularities  as  purely  the  result  of  subaerial  agencies  as  in 
the  driftless  region  itself.  This  is  quite  evident  along  both  sides  of 
the  valley  of  the  "Wisconsin  from  Stevens  Point  to  the  north  line  of 
the  district,  and  along  the  valleys  of  its  principal  western  tributaries. 
All  along  the  line  of  the  Wisconsin  Valley  Kailroad,  between  Knowl- 
ton  and  Grand  Rapids,  wherever  the  least  cutting  is  made  the  rock 
is  laid  bare.  Farther  west,  on  the  divide  between  the  Yellow  and 
Black  rivers,  in  Clark  and  western  Wood  counties,  there  is  a  consid- 
erable thickness  of  drift  material,  which,  however,  presents  none  of 
the  heaped  up  appearance  characteristic  of  the  more  eastern  drift- 
bearing  regions. 

The  linear  topography  above  mentioned  is  generally  found  best 
marked  in  the  regions  east  of  the  belt  along  which  the  drift  materials  have 
their  most  marked  morainic  development.  As  shown  hereafter,  this 
belt  lios  usually  not  far  east  from  the  western  limit  of  the  drift  region. 


PLATE,  XXVTA 


GEOLOGICAL   MAP 

('/•//;/• 

FOUR    T.AKK    COrNTRY    of    DANK    COrNTY 

({r.iif/nert  If*  xfitnr  the 

DIRECTIONS  andEFFECrrs  of  the  GLACIAL  AFOXTiMK  XT 

I*.  D.  Irving 
1876. 


.      .  .--         •  •  '  /  »      //        A  / 


Tn-ntm Limexloiif          •Sl.Petrr.iSanti.itone.  Lawer^tagiir.iianLintrst!inr,MadisfitX-Mriiilotii Brtb.n>tadam$umt.ii<<nr 


eii  of  glarial  movement 


GiacieUStritu 


THE  GLACIAL  DRIFT.  613 

In  the  Four  Lake  Country  of  Dane  county  the  linear  arrangement 
is  finely  marked,  its  directions  coinciding  with  the  directions  of  the 
glacial  striee  on  the  underlying  rocks.  'Lakes  Mendota  and  Monona, 
and  Lake  Waubesa,  in  part,  lie  in  N.E.— S.W.  valleys,  the  first 
named  occupying  two  such  valleys,  which  are  partly  separated  by  the 
rock  ridge  of  Picuic  and  MacBride's  points.  The  valley  of  Lake  Mo- 
nona extends  several  miles  to  the  southeastward  beyond  the  lakes, 
preserving  its  direction,  which,  like  that  of  the  two  valleys  of  Lake 
Mendota,  is  about  S.  57°  E.,  or  parallel  to  the  direction  of  the  striae 
to  be  seen  at  the  large  quarries  west  of  Madison.  Numerous  other 
similar  valleys  of  varying  size  are  to  be  seen  in  the  same  country, 
some  occupied  by  marshes  or  streams,  others  entirely  dry.  Harrow 
detached  ridges,  lines  of  marsh,  and  the  outlines  of  the  formations 
show  the  same  arrangement,  and  the  same  coincidence  with  the  di- 
rections of  the  striae. 

Plate  XXVI  A  is  a  geological  map  of  the  Four  Lake  Country,  and 
is  designed  to  show  especially  how  the  areas  of  the  several  formations 
have  been  carved  out  by  the  glacial  forces;  since  the  formations  lie 
one  above  the  other  nearly  horizontally,  the  map  is  also  to  some  ex- 
tent a  topographical  one.  It  gives  also  the  directions  of  the  striae 
observed  at  different  points,  and  the  lines  along  which  they  indicate 
the  glacial  movement  to  have  taken  place.  It  will  be  observed  that 
the  glacial  striae  vary  in  direction  from  due  south  at  the  southeast 
corner  of  the  map  to  nearly  west  at  its  northwest  corner,  and  that 
the  linear  outlines  of  the  formation  areas,  lake  valleys,  etc.,  keep  pace 
with  this  change  in  direction.  The  Atlas  map  of  Area  D,  which 
shows  also  the  marsh  and  stream  directions,  etc  ,  and  is  on  a  larger  scale, 
as  well  as  more  accurately  drawn,  brings  this  interesting  relation  out 
even  more  strikingly. 

It  would  be  instructive  to  describe  in  some  detail  the  different 
linear  valleys,  ridges  and  outlines  of  this  district,  tracing  their  vary- 
ing directions,  but  the  space  at  command  forbids  this.  It  may  be 
mentioned  that  in  the  town  of  Springfield  a  single  narrow  valley, 
carved  out  in  the  Lower  Magnesian  to  a  depth  of  100  feet,  is  to  be 
observed  curving  gradually  westward  to  correspond  with  a  slight 
change  in  the  direction  of  the  striae  011  its  sides. 

O 

ISTorlh western  Dane  and  eastern  Columbia  counties  are  level  com- 
pared with  the  district  just  described,  but  the  linear  arrangement  is 
very  plainly  marked  in  lines  of  marsh,  streams  and  geological  out- 
lines, as  will  be  seen  readily  from  an  inspection  of  the  maps  of  areas 
D.  and  E.  Fig.  52  gives  the  shape  of  the  area  of  Trenton  limestone 
which  occupies  the  towns  of  York  and  Columbus,  extending  also  into 


614 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


adjoining  towns  on  the  east  and  west.  A  number  of  short  parallel 
ridges  are  to  be  seen  in  the  same  region,  some  of  which  are  rock,  and 
others  either  altogether  of  drift  or  at  least  with  a  core  only  of  rock. 

Roches  moutonees,  so  characteristic  of  all  glaciated  regions  where 
the  underlying  formation  is  of  the  hard  crystalline  rocks,  are  not  en- 
tirely wanting  in  Central  Wisconsin.  The  bald  and  smooth  rounded 
summits  of  quartzite  so  conspicuous  on  the  high  bluffs  of  Caledonia, 
Columbia  county,  show  the  structure  finely.  These  summits  have  a 
direction  but  little  south  of  west,  coinciding  with  the  directions  of 
of  the  striae  upon  them.  The  scattering  knobs  of  granite  and  por- 

FIG.  52. 


OUTLINE  OP  AN  ABBA  or  TRENTON  LIMESTONE  NEAR  COLUMBUS. 
Scale  4  miles  to  1  inch. 

phyry  which  rise  through  the  Potsdam  sandstone  in  Columbia,  Mar- 
quette,  "Waushara  and  Green  Lake  counties  are  all  distinctly  "  sheep's 
backs."  The  main  Archaean  region  of  Central  Wisconsin,  stretching 
westward  from  the  Wisconsin  to  Black  river,  does  not  show  any  dis- 
tinct "  roch.es  moutonees,"  it  being  to  the  west  of  the  region  of 

f  CT  o 

greatest  glaciation.  Further  east,  in  Shawano  and  adjoining  counties, 
these  shapes  would  be  expected.  The  Silurian  strata  of  Central  Wis- 
consin are  either  too  fragile  or  too  susceptible  to  the  solving  action 
of  the  atmospheric  waters,  to  have  received  or  retained  the  "  roche 
moutoneo  "  shape. 


THE  GLACIAL  DRIFT.  615 

Drift  hills  and  ridges  occur  over  all  of  the  drift-bearing  area  of 
Central  AVisconsin.     In  the  region  north  of  the  east  and  west  drift 
limit,  in  Marathon,  Wood,  and  Clark  counties,  they  do  not,  however, 
show  any  distinct  morainic  character;  but  in  Dane,  Sank,  Columbia, 
eastern  Adams,  Marquette,  Grreen  Lake,  AVaushara,   Waupaca   and 
Portage  counties,  they  show  this  character  in  a  marked  degree.  More- 
over, there  is,  in  these  counties,  a  certain  belt  of  country,  the  western 
border  of  which  is  never  very  far  from  the  eastern  edge  of  the  drift- 
less  area,  in  which  the  "  knobby  "  drift  hills  reach  an  unusual  de- 
velopment, the  drift  materials  are  thicker  than  elsewhere,  and  the 
surface  of  the  country  is  dotted  with  circular  or  winding  depressions, 
without  outlet,  of  very  varying  size,  and  often  occupied  by  ponds  or 
lakes.     To  these  depressions,  in  certain  other  parts  of  Wisconsin, 
where  they  are  to  be  recognized  on  a  still  larger  scale,  the  name  of 
"  potash  kettles"  has  been  applied,  in  allusion  to  their  common  shape; 
and  the  belt  of  country  in  which  they  occur  has  been  designated  as 
the  " Potash  Kettle  Range,"  or,  more  simply,  the  "Kettle  Range." 
These   latter    names   have  heretofore  been   applied   especially   to  a 
narrow  and   very  marked  range  which  follows  the   divide  between 
the   valley  of    Lake    Michigan   and  that  in    which   lie  Green  Bay, 
Lake    Winnebago,    and   the    head   waters    of    Rock   river.      Prof. 
Chamberlin  has  traced  this  belt  southward  to  the  northeastern  part  of 
Rock  county,  where  he  .finds  it  bifurcating,  one  branch  running  south- 
eastward into  Illinois,  whilst  the  other,  curving  west  and  northwest, 
enters  the  Central   Wisconsin   district  on   the   south  line  of   Dane 
county,  in  the  towns  of  Rutland  and  Dunkirk. 

From  the  south  line  of  Dane  county  northward,  the  "  Kettle  Range" 
is  now  recognized  for  the  first  time,  having  been  traced  for  a  distance 
of  over  120  miles,  as  far  as  the  line  of  the  Wisconsin  Central  Rail- 
road, in  Portage  and  Waupaca  counties;  beyond  which  it  is  known 
to  extend  until  it  becomes  merged  into  the  great  accumulations  of 
morainic  drift  which  stretch  from  the  head  waters  of  the  Wolf  and 
Oconto  rivers  westward,  over  a  large  part  of  the  Archaean  region  of 
the  north  part  of  the  state.  The  Central  Wisconsin  "  Kettle  Range  " 
reaches  in  parts  a  much  greater  width  than  that  of  the  eastern  part  of 
the  state,  and  its  inner  edge  is  not  so  well  defined.  These  differences, 
however,  admit  of  a  satisfactory  explanation.  Plate  XXYI  shows 
the  position  of  the  Central  Wisconsin  Range,  whose  course  and  char- 
acter are  described  in  more  detail  in  what  follows. 

Beginning  on  the  south,  we  find,  in  the  towns  of  Rutland,  T.  5,  R. 
10  E.,  western  Dunkirk,  T.  5,  R.  11  E.,  and  northeastern  Oregon, 
T.  5,  R.  9  E.,  a  considerable  development  of  knolls  and  ridges  of 


616  GEOLOGY  OF  CENTRAL  WISCONSIN. 

gravel,  with  a  number  of  depressions  occupied  by  small  lakes,  one  of 
which,  on  Sec.  3,  T.  5,  II.  10  E.,  is  a  mile  in  length.  The  belt  in  these 
towns  has  a  width  of  about  eight  miles,  and  a  course  west  of  north. 
In  southwestern  Dunn,  T.  6,  E.  10  E.,  and  Fitchburg,  T.  6,  R.  9  E., 
a  bow  is  made  to  the  westward,  the  convex  side  of  which  reaches  the 
northwest  part  of  Oregon,  where  knolls  and  large  well  marked  dry 
kettles  are  to  be  seen,  and  the  width  is  not  more  than  from  4  to  6 
miles.  In  southwestern  Madison,  T.  7,  R.  9  E.,  the  inner  edge  of  the 
belt  reaches  the  western  ends  of  Lakes  Monona  and  Mendota,  where 
are  finely  marked  mammillary  knolls,  rising  50  to  75  feet  above  the 
lakes,  and  arranged  in  lines  transverse  to  the  axes  of  the  lake  valleys. 
The  western  side  of  this  part  of  the  belt  is  on  the  high  ground  of 
Middleton  prairie,  where  kettles  and  knolls  are  to  be  seen  at  an  ele- 
vation of  300  and  more  feet  above  the  Madison  lakes.  The  same  is 
true  of  the  low  ground  of  northeastern  Middleton,  where  is  quite  a 
cluster  of  water-filled  kettles.  From  Middleton  the  range  passes  into 
Springfield,  T.  10,  R.  8  E.,  where  the  best  development  is  in  the 
northwest  corner,  and  the  width  is  some  four  miles.  The  high  divide 
between  the  Wisconsin  and  Catfish  rivers  is  crossed  in  the  adjoining 
portions  of  Springfield,  Dane,  T.  11,  R.  8  E.,  Berry,  T.  10,  R.  7  E., 
and  Roxbury,  T.  11,  R.  7  E.  In  Roxbury  the  belt  descends  abrupt- 
ly 200  feet  into  the  low  ground  of  the  valley  of  the  Wisconsin.  Hand- 
somely shaped  and  deep  kettles  are  seen  in  Roxbury,  on  Sections  8,  9 
and  16  in  a  low  area,  surrounded  by  eleven  entirely  isolated  rock 
bluffs,  and  two  quite  large  kettle  lakes  are  found  on  the  north  side  of 
the  town.  Columbia  county  is  entered  in  the  town  of  West  Point, 
T.  12,  R.  7  E.,  where  the  same  characters  as  observed  in  Roxbury 
are  continued. 

The  Kettle  Range  crosses  the  Wisconsin  river  in  the  northern  part 
of  the  town  of  West  Point,  and  continuing  northward  along  the  east 
side  of  Sauk  prairie,  reaches  the  foot  of  the  Baraboo  bluffs  in  T.  11, 
R.  6  E.,  and  T.  11,  R.  7  E.,  Sauk  county.  On  top  of  the  bluffs  im- 
mediately north  of  here  it  is  not  well  marked,  but  in  the  gorge  in 
which  lies  Devil's  Lake,  and  which  makes  a  complete  cut  through  the 
range,  are  very  large  accumulations  of  drift  materials.  The  lake  it- 
self really  occupies  a  kettle  depression,  being  held  in  position  by  im- 
mense heaps  of  entirely  unmodified  drift  at  each  extremity.  These 
hills  rise  over  100  feet  above  the  surface  of  the  lake,  the  southern  one 
falling  off  on  the  side  away  from  the  lake  to  over  150  feet,  and  tho 
northern  one  fully  100  feet,  below  its  level.  The  thickness  of  the 
drift  in  the  gorge  must  be  nearly,  if  not  more  than,  300  feet  It  has 
been  shown  on  a  previous  page,  that  in  this  gorge  we  have,  in  all 


THE  GLACIAL  DRIFT.  617 

probability,  an  ancient  erosion  channel  of  the  Wisconsin  river,  which, 
becoming  blocked  during  the  glacial  times,  was  never  after  regained. 
The  Devil's  Lake  drift  appears  to  lie  on  the  western  edge  of  the  Ket- 
tle Range,  no  marked  development  of  which  is  to  be  seen  on  top  of 
the  bluff  for  two  miles  east,  when  knolls  of  limestone,  pebbles,  and 
erratics  of  large  size,  are  met  with  at  the  greatest  elevations. 

Northward  from  Devil's  Lake  the  Range  traverses  the  Baraboo 
valley  —  in  which  large  heaps  of  unmodified  drift  occur  near  the  vil- 
lage of  the  same  name  — and  passing  thence  through  northern  Sauk 
county,  crosses  the  Wisconsin  into  northwestern  Columbia  (Newport 
und  Lewiston),  and  southeastern  Adams.  Here  begins  the  great  de- 
velopment of  kettles,  both  dry  and  lake-filled,  which  is  continued 
northward  —  the  width  of  the  whole  range  at  the  same  time  greatly 
expanding  —  through  northwestern  and  northern  Marquette,  "Wan- 
phara,  eastern  Portage,  and  western  Waupaca  counties,  to  the  line  of 
the  Wisconsin  Central  railroad,  and  for  an  indefinite  distance  in  the 
less  settled  and  unsettled  regions  beyond.  In  Waushara  county,  the 
Range  has  attained  a  width  of  fully  five  and  twenty  miles,  the  kettles, 
lakes,  knolls  and  ridges  lying  thickly  spread  over  the  whole  surface. 
As  instances  of  finely  marked  kettles,  may  be  mentioned  those  that 
occur  very  numerously  over  the  town  of  Springfield,  Marquette 
county,  and  in  the  eastern  part  of  Lincoln,  Adams  county.  These 
are  for  the  most  part  dry,  often  quite  perfectly  circular,  50  feet  in 
depth  and  500  feet  in  width  at  top.  They  occur  quite  up  to  the  edge 
of  the  driftless  area,  and  within  a  mile  of  one  of  the  fragile  sandstone 
towers  of  that  district  —  Pilot  Knob.  The  elevation  above  Lake 
Michigan  is  550  feet.  Excellent  illlustrations  of  lake-filled  kettles 
are  to  be  found  in  the  very  numerous  lakes  of  the  towns  of  Marion, 
Mount  Morris,  and  Springwater,  Waushara  county.  Some  of  these 
are  of  quite  large  size,  as,  for  instance,  Silver  lake,  near  Wautoma, 
which  is  over  a  mile  in  length.  They  lie  quite  often  in  deep  depres- 
sions, the  water  level  not  urifrequently  standing  at  25  to  40  feet  below 
the  top  of  the  banks,  which  are  wholly  of  gravel,  and  very  steep,  in 
some  cases  almost  perpendicular.  Two  or  more  lakes  commonly 
occur  close  together,  the  bank  between  them  having  a  width  on  top 
scarcely  enough  for  a  wagon  road,  and  a  steep  descent  to  the  water 
on  either  side.  This  is  finely  shown  in  the  case  of  Silver  Lake,  al- 
ready cited,  and  the  nearly  as  large  and  partly  peat-filled  lake  imme- 
diately north  of  it.  The  average  elevation  of  the  country  in  which 
ill  of  these  lakes  lie  is  about  400  feet,  and  the  country  between  them 
is  everywhere  pitted  with  smaller  dry  kettles. 

Further  west,  in  Waushara  county,  in  the  towns  of  Coloma,  Rich- 


CIS  GEOLOGY  OF  CENTRAL  WISCONSIN. 

ford,  DeerfieM  and  Rose,  is  a  belt  of  greater  altitude,  550  to  consid- 
erably over  600  feet  above  Lake  Michigan.  Here  the  lakes  are  less 
abundant,  the  drift  taking  on  rather  the  character  of  ridges  and  knolls, 
though  tortuous  dry  kettles  are  frequent.  This  ridge  region  is  the 
divide  between  the  waters  of  the  Fox  and  Wisconsin  rivers,  and  the 
drift  depositions  within  it  seem  to  have  suffered  little  modification 
since  their  first  formation.  The  roads  running  eastward  from  Colo- 
ma,  on  Burr  Oak  prairie,  pass  over  parts  of  this  great  morainic  heap 
where  its  structure  and  nature  are  seen  to  great  advantage. 

For  further  ideas  as  to  the  Kettle  Range,  its  position,  varying 
width,  and  great  numbers  of  lakes,  as  compared  with  the  other  parts 
of  the  state,  reference  should  be  made  to  Plate  XXYI.  The  lakes  on 
this  plate  are  all,  except  mill  ponds,  that  are  given  on  the  township 
plats  of  the  region  mapped,  and  are  accurately  placed,  although  the 
map  is  of  so  small  scale.  No  doubt,  others,  not  on  the  plats,  occur  in 
considerable  numbers. 

The  materials  of  the  drift  are  bowlders,  gravel,  sand  and  clay. 
Bowlders  are  scattered  thickly  over  the  whole  surface  of  the  drift 
region.  Nearly  all  are  of  some  sort  of  crystalline  rock,  sandstone  oc- 
curring very  rarely,  and  limestone  —  except  as  large  sized  pebbles  — 
still  more  rarely.  Of  the  crystalline  rock  bowlders,  those  of  gneiss 
of  some  form  or  other  greatly  predominate,  making  up  50  to  75  per 
cent,  of  all.  Next  in  abundance  to  the  true  gneiss  bowlders,  are  those 
of  some  form  of  brown-weathering,  hornblendic  rock,  which  is  gen- 
erally syenite,  and  nearly  always  gneissoid  in  texture.  Of  80  erratics 
counted  within  a  few  rods  along  the  lake  shore  of  the  University  farm 
at  Madison,  44  were  gneiss,  15  gneissoid  syenite,  9  granite,  3  diorite, 
2  red  porphyry,  2  quartzite,  2  sandstone,  1  red  felsite,  1  granulite 
and  1  fine-grained  slate.  Whilst  other  rocks  are  often  included,  these 
numbers  express,  in  a  general  way,  what  is  true  for  the  whole  region. 
The  gneiss  bowlders  vary  much  in  mineralogical  composition  and 
closeness  of  grain,  but  are  nearly  always  very  distinctly  laminated, 
and  often  much  contorted.  Occasionally  they  run  into  mica  slates  on 
the  one  hand,  and  gneissoid  granite  on  the  other.  The  granite 
bowlders  vary  also,  but  pink  orthoclase  granites  are  most  common. 
All  over  the  region,  from  Dane  northward  to  Waushara,  and  prob- 
ably far  beyond,  red  porphyry  and  compact  red  felsite  bowlders  are 
very  noticeable  from  their  bright  red  color,  although  forming  only  a 
small  proportion  of  the  whole  number  of  erratics.  They  include 
kinds  in  which  there  is  a  compact  red  felsitic  matrix,  with  dissemi- 
nated hyaline  and  amygdaloidal  quartz;  others  in  which  both  quartz 
and  felspar  are  porphyritic;  others  in  which,  in  addition  to  these,  the 


THE  GLACIAL  DRIFT.  619 

red  matrix  itself  develops  large  crystalline  faces;  and  still  others  in 
which  the  aphanitic  matrix  constitutes  the  whole  rock. 

Quartzite  bowlders  are  not  at  all  common  except  in  one  or  two  lim- 
ited districts.  One  of  these  is  in  eastern  Dane  county,  in  the  towns 
of  Medina  and  Deerfield,  where  they  are  abundant,  and  associated 
with  bowlders  of  conglomerate,  both  having  beyond  doubt  come  from 
a  mound  of  quartzite  a  few  miles  northeast  in  Dodge  county.  It 
might  be  expected  that  the  Baraboo  quartzite  ranges  would  have  had 
their  rock  scattered  very  widely  in  the  country  to  the  southward,  but 
this  is  not  the  case.  In  the  Baraboo  valley,  and  still  more  in  the 
country  immediately  south  of  the  ranges,  quartzite  bowlders  of  large 
size  are  very  abundant.  Further  south  they  occur  sparingly  as  far 
as  the  region  about  Lodi,  including  talcose  quartz-slate,  also  undoubt- 
edly from  the  Baraboo  ranges.  Still  further  south  they  are  more  no- 
ticeable for  their  absence  than  their  presence.  It  will  be  seen  that 
this  rather  unexpected  fact  admits  of  a  very  satisfactory  explanation. 
Sandstone  bowlders  are  rare,  not  because  sandstone  is  not  abundant 
in  the  regions  over  which  the  drift  movement  took  place,  but  because  of 
the  very  friable  nature  of  the  rock.  Those  sandstone  bowlders  that  are 
found  are  always  either  somewhat  quartzitic,  or,  as  is  more  frequent- 
ly the  case,  are  rendered  hard  by  a  large  amount  of  cementing  brown 
iron  oxide.  Amongst  the  smaller  materials  of  the  drift  are  sometimes 
found  hard  ferruginous  concretions  which  are  recognized  as  coming 
from  the  great  sandstone  region  of  the  heart  of  the  state.  That  large 
limestone  bowlders  should  be  so  very  rare  appears  to  be  due  to  the 
ease  with  which  that  rock  is  worn  into  smaller  sizes. 

One  of  the  most  interesting  substances  found  in  the  drift,  though 
hardly  attaining  the  size  of  a  bowlder,  is  the  native  copper,  which  is 
found  in  fragments  widely  scattered  over  the  northwest,  from  Ohio  to 
Minnesota.  These  native  copper  fragments  are  far  more  abundant 
in  Wisconsin  than  elsewhere,  and  far  more  abundant  there  than  is 
commonly  supposed.  Specimens  weighing  from  a  few  ounces  up  to 
30,  40,  and  even  50  pounds,  are  constantly  found  in  digging.  The 
late  Dr.  Lapham  informed  me  that  the  coppersmiths  in  Milwaukee 
purchased  from  tinders  yearly  several  hundred  pounds  of  this  copper. 
Ancient  implements  of  copper  have  been  found  very  abundantly  in 
Wisconsin,  the  largest  collection  of  such  relics  in  the  world  now  being 
in  possession  of  the  State  Historical  Society  at  Madison.  It  has  been 
argued  that  these  implements  prove  a  high  degree  of  civilization  for 
the  races  that  occupied  the  northern  United  States  in  remote  times, 
since  copper  smelting  is  an  art  unknown  to  the  more  barbarous  peo- 
ples. It  is  evident  enough,  however,  that  there  is  a  direct  connection 


620  GEOLOGY  OF  CENTRAL  WISCONSIN. 

between  the  abundance  of  copper  implements,  and  the  abundance  of 
drift  copper  fragments,  which  in  ancient  times  were  probably  much 
more  plenty  on  the  surface  than  now,  and  which  by  pounding  could 
yield  any  and  all  of  the  implements  ever  found.  Even  a  simple  melt- 
ing down  was  unnecessary,  and  is  directly  disproved  by  the  occur- 
rence on  the  tools  of  unalloyed  silver.  Some  of  the  copper  for  these 
ancient  implements  may  have  been  obtained  directly  from  its  home 
in  the  rock,  on  the  shores  of  Lake  Superior,  but  this  required,  of 
course,  no  more  smelting  than  the  drift  fragments. 

In  size  the  bowlders  vary  much,  but  there  is  generally  a  marked 
break  in  size  between  them  and  the  "pebbles,"  the  latter  being  pre- 
dominatingly of  limestone,  the  former  of  crystalline  rocks  of  various 
kinds.  In  general  the  largest  bowlders  are  found  farther  north.  In 
the  southern  part  of  the  district  the  larger  ones  run,  commonly,  from 
two  to  four  feet  in  diameter,  rarely  exceeding  the  latter  ligure,  though 
occasionally  running  to  as  much  as  10  feet  in  one  dimension.  In 
Waushara  county,  especially  on  the  eastern  flank  of  the  Kettle  Range, 
bowlders  5  to  10  feet  in  diameter  are  very  plenty,  occurring  sometimes 
in  thick  clusters,  as  on  the  hill  immediately  north  of  the  village  of 
Poysippi,  and  in  several  other  places  in  the  neighborhood,  where  many 
of  one  kind  are  found,  giving  rise  to  some  doubt  as  to  the  possible  ex- 
istence of  the  rock  in  place.  The  largest  bowlder  observed  anywhere  in 
the  district  lies  at  the  edge  of  a  wood  on  the  S.  E.  qr.  of  Sec.  16,  T.  18, 
R.  11  E.,  "VVaushara  county.  It  is  a  red  granite,  sharp-angled,  13^- 
feet  high,  30  feet  long,  and  22  wide,  measures  110  feet  in  circumfer- 
ence, is  buried  in  its  lower  part  to  an  unknown  extent,  and  came  from 
a  large  outcrop' about  four  miles  east.  In  shape,  the  smaller  bowlders 
are  often  very  much  rounded,  the  angularity  increasing  with  the  size, 
but  depending  also  much  upon  composition,  hornblendic  bowlders  al- 
ways showing  more  rounding.  Scratched  and  polished  bowlders  are 
often  seen,  but  do  not  form  any  large  proportion,  and  are  generally  of 
the  harder  and  less  destructible  rocks,  such  as  quartziteand  granite. 

With  regard  to  the  distribution  of  bowlders,  it  may  be  said  that, 
whilst  scattered  widely  over  the  whole  region,  they  are  more  plenty 
in  the  northern  than  in  the  southern  portions  of  the  district,  and 
are  especially  numerous  along  the  inner  (eastern)  edge  of  the  Ket- 
tle Range.  The  greatest  development  of  bowlders  noticed  in  Cen- 
tral Wisconsin  was  in  eastern  Waushara  county,  and  in  the  adjoin- 
ing portions  of  Portage  and  Waupaca.  North  of  the  village  of 
Poysippi,  as  already  stated,  the  hill  is  thickly  studded  with  immense 
bowlders  of  a  coarse,  knotty  gneiss,  composed  chiefly  of  black  mica 
and  pink  felspar.  In  the  town  of  Rose,  T.  20,  R.  10  E.,  the  slope 


THE  GLACIAL  DRIFT.  621 

eastward  from  the  high  prairie  of  the  next  town  to  the  west  is  strewn 
with  immense  bowlders  in  a  very  striking  manner,  and  the  same  thing 
is  to  be  observed  twelve  to  fifteen  miles  further  north,  alonor  the  lines 

O 

of  the  Wisconsin  Central  and  Green  Bay  and  Minnesota  railroads, 
east  of  Am  hers t  Junction.  Clusters  of  bowlders  are  very  common, 
even  much  further  south,  as  in  the  central  part  of  the  town  of  Mar- 
cellon,  Columbia  county,  and  in  the  S.  E.  qr.  of  Sec.  3,  Deerfield, 
Dane  county,  where  the  bowlders  are  scarcely  more  than  ten  feet 
apart,  over  an  area  of  some  10  to  15  acres.  When  these  clusters  oc- 
cur, they  are  very  apt  to  be  mostly  of  one  kind.  Altitude  has  evi- 
dently had  no  influence  whatever  on  the  distribution  of  bowlders,  since 
they  are  found  on  the  highest  and  lowest  parts  of  the  country,  indif- 
ferently. East  of  Devil's  Lake,  in  the  towns  of  Greenfield  and  Mer- 
rimack,  they  are  found  in  abundance  and  of  large  size  on  the  highest 
est  portion  of  the  Baraboo  bluffs,  at  altitudes  of  over  900  feet  above 
Lake  Michigan.  Bowlders  are  found,  also,  on  the  tops  of  all  the  iso- 
lated bluffs  that  occur  within  the  drift-bearing  area.  Very  large 
hornblendic  erratics,  for  instance,  are  to  be  seen  on  the  very  summit 
of  the  limestone  bluff  of  the  northwestern  part  of  the  town  of  Spring- 
field, Marqnette  county.  This  bluff  lies  on  the  top  of  the  divide  be- 
tween the  waters  of  the  Fox  and  Wisconsin  rivers,  has  a  height  above 
its  base  of  200  feet,  and  a  total  altitude  of  730  feet  above  Lake  Mich- 
igan. It  lies  on  the  western  edge  of  the  Kettle  Range,  and  a  mile  or 
two  west,  in  a  country  200  to  250  feet  lower,  the  drift  has  ceased  alto- 
gether. 

Gravel  makes  up  a  large  part  of  the  drift  accumulations,  though  not 
so  great  a  proportion  as  the  sand.  Two  general  kinds  of  gravel  may 
be  noted,  the  coarse  and  the  fine,  the  former  occurring  more  especially 
in  those  regions  where  the  drift  appears  to  take  on  a  true  morainic 
character,  forming  knolls  and  ridges,  and  the  sides  of  many  of  the 
depressions  of  the  Kettle  Range,  whilst  the  finer  gravel  is  met  with 
commonly  in  the  valleys  of  streams,  or  wherever  a  distinct  stratified 
arrangement  of  the  loose  materials  is  perceptible.  The  coarse  gravel 
is  for  the  most  part  of  limestone  pebbles,  with  which  are  mingled 
some  pebbles  of  white  chert,  and  some  of  various  crystalline  rocks, 
which  increase  in  quantity  towards  the  north.  The  ordinary  limestone 
pebbles  are  of  a  white  color,  run  from  three  or  four  to  eight  or  ten 
inches  in  diameter,  are  commonly  oblong  in  shape,  much  rounded  at 
the  ends,  and  often  have  one  or  two  sides  smoothed  and  striated.  Not 
unfrequently  fossils  are  contained,  indicating  the  origin  of  the  peb- 
bles, which  is  also  to  be  inferred  from  their  lithological  characters. 
The  coarse  unstratified  gravel  is  widely  distributed  over  all  the  region 


622  GEOLOGY  OF  CENTRAL  WISCONSIN.' 

east  of  the  drift  limit  and  south  of  the  line  of  the  Wisconsin  Central 
railroad,  in  Portage  and  Waupaca  counties,  and  also  to  an  indefinite 
distance  further  north.  It  is  most  abundant  in  the  Kettle  Range  it- 
self, but  is  not  entirely  restricted  to  it.  Even  northward,  into  the 
region  of  the  Archaean  rocks,  the  gravel  is  partly  of  limestone  peb- 
bles, which  have  been  brought  from  the  limestone  formations  to  the 
eastward.  In  the  region  north  of  the  driftless  area  and  west  of  the 
Kettle  Range  —  including  the  valley  of  the  Wisconsin  as  far  north 
as  the  northern  line  of  Marathon  county,  and  the  country  lying  be- 
tween the  Wisconsin  and  Black  rivers,  in  northern  Wood,  and  in 
Marathon  and  Clark  counties  —  whilst  erratics  are  often  seen,  some- 
times in  clusters  of  very  large  bowlders,  the  coarse  limestone  gravel 
appears  wholly  wanting.  The  fine  gravel  consists,  more  largely  than 
the  coarse,  of  pebbles  of  quartz  and  various  crystalline  rocks.  It  is 
to  be  seen,  finely  stratified,  in  the  drift  of  stream  valleys,  and  in  some 
places  far  away  from  the  streams,  as,  for  instance,  on  the  divide  be- 
tween Black  and  Yellow  rivers,  where  it  occurs  interstratified  with 
sand  and  clay  to  a  thickness  of  over  100  feet. 

Sand  appears  to  make  up  by  far  the  largest  part  of  the  drift  de- 
posits. It  is  commonly  light-colored  and  purely  silicious,  but  is  often 
mingled  with  more  or  less  clayey  material,  both  when  in  the  plainly 
stratified  and  the  more  or  less  unstratified  conditions.  Occasionally 
it  is  stained  brown  with  hydrous  iron-oxide,  and  when  stratified  alter- 
nates in  different  colored  bands.  The  explanation  of  the  large  pre- 
ponderance of  sand  over  clay  in  the  Central  Wisconsin  drift  will  ap- 
pear hereafter. 

Clay  occurs,  as  already  said,  to  a  considerable  extent  mingled  with 
the  sand,  over  which  it  sometimes  preponderates  greatly,  forming  a 
firm,  tenacious  clay,  which  is  stuck  full  of  scratched  and  polished  peb- 
bles and  bowlders,  and  appears  to  be  identical  with  the  ''  till "  of  the 
Scotch  geologists.  Such  a  clay,  however,  is  not  often  to  be  seen. 
Something  like  it  appears  in  the  heaps  that  lie  on  the  high  prairies 
of  northern  Dane  and  southern  Columbia,  but  the  only  places  where 
an  apparently  true  till  has  been  noticed  are  in  the  vicinity  of  Devil's 
Lake,  for  a  better  understanding  of  whose  position  reference  should 
be  made  to  Plate  XIX,  and  the  descriptions  accompanying  it.  The 
lake  lies  in  a  perpendicularly  walled  gorge,  500  to  600  feet  deep, 
which  passes  entirely  through  the  main  quartzite  range  of  the  Bara- 
boo.  This  gorge  is  about  three-quarters  of  a  mile  in  width,  and  be- 
tween three  and  a  half  and  four  miles  in  length.  At  the  northern 
end  its  course  is  nearly  due  north  and  south  for  over  a  mile,  when  it 
turns  nearly  at  right  angles,  and  runs  for  the  rest  of  its  length  but 


THE  GLACIAL  DRIFT.  623 

little  south  of  east.  Devil's  Lake  lies  in  the  north  and  south  portion 
of  the  gorge.  At  its  northern  end  a  hill  of  drift  rises  abruptly  from 
the  water  to  a  height  of  100  feet,  falling  on  the  further  side  as  ab- 
ruptly over  200  feet  to  the  Baraboo  river.  A  short  distance  beyond 
the  southern  end  of  the  lake  a  similar  hill  chokes  the  gorge  from  side 
to  side,  rising  100  feet  from  the  lake  level,  and  on  the  eastern  side 
sinking  rapidly  until  at  its  eastern  end  the  bottom  of  the  gorge  is 
full  150  feet  below  the  lake.  Through  this  hill  a  deep  cutting  is 
made  for  the  Chicago  and  Northwestern  Railroad.  The  sides  of  the 
cutting  show  no  sign  of  stratification,  but  only  a  sandy  tenacious  clay 
with  numerous  scratched  pebbles  and  bowlders,  the  latter  including 
the  usual  kinds  of  crystalline  rocks,  but  also  a  number  of  quartzite, 
some  of  which  are  much  smoothed  and  striated.  The  large  drift  cut- 
ting near  Baraboo  shows  something  the  same  sort  of  material,  which 
is,  however,  much  more  sandy,  and  has  traces  of  a  crude  stratification. 
It  is  quite  probable  that  till -like  clays  occur  somewhat  widely  in  the 
region  of  the  Kettle  Range,  but  the  rare  cuttings  make  this  conject- 
ural only.  In  southeastern  Adams  county,  in  the  region  about  Big 
Spring,  quite  a  large  area  occurs  in  which  the  surface  material  is  a 
red  tenacious  clay.  ~No  cutting  was  seen  in  this  clay,  and  its-  exact 
relations  and  structure  are  doubtful. 

Stratified  clays,  often  fine-laminated,  are  found  in  the  valleys  of 
most  of  the  streams  in  the  southern  part  of  the  Central  Wiscon- 
sin district,  where  they  are  interstratified  with  fine  gravel  and 
sand,  and  are  often  utilized  for  making  brick.  Such  clays  are  found 
at  a  number  of  places  in  the  Catfish  Valley,  as,  for  instance,  in  the 
vicinity  of  Madison,  at  Oregon,  at  Stoughton,  etc.,  at  times  yielding 
a  pure  white  or  cream  colored  brick,  at  others,  an  ordinary  red  brick. 
The  following  analysis  is  of  one  of  the  latter  kind,  from  a  pit  in  the 
valley  through  which  the  Milwaukee  &  St.  Paul  railroad  passes,  on 
the  S.  E.  qr.  of  Sec.  17,  T.  7,  R.  9  E.,  about  one  mile  west  of  the 
University  at  Madison:  silica,  75.80;  alumina,  11.07;  iron  peroxide, 
3.53;  iron  protoxide,  0.31;  lime,  1.84;  magnesia,  0.08;  carbonic  di- 
oxide, 1.09;  potassa,  1.14;  soda,  0.40;  water,  1.54;  hygroscopic  moist- 
ure, 2.16=99.56. 

These  clays  contain  occasionally  small  pebbles  of  limestone  which, 
on  being  baked  in  the  middle  of  the  brick  will  subsequently  "  slack  " 
and  cause  it  to  burst  open.  The  clays  that  produce  the  light  or 
cream-colored  brick  contain  not  unfrequently  as  much  iron  as  the 
ordinary  red  clays,  but  are  very  much  more  calcareous,  resembling  in 
this  regard  the  famous  Milwaukee  brick  clay. 

The  different  behaviours  of  these  two  classes  of  clay  under  heat  is 


624:  GEOLOGY  OF  CENTRAL  WISCONSIN. 

evidently  due  largely  to  the  difference  in  amount  of  lime  and  magne- 
sium carbonates,  but  is  not  well  understood. 

An  attempt  to  study  out  the  system  of  arrangement  of  the  drift 
materials  meets  with  no  little  difficulty  from  the  rarity  of  natural 
or  artificial  sections.  Enough  information  can,  however,  be  obtained 
from  the  few  sections  that  do  occur,  and  from  records  of  well-boriners, 

'  2r>     / 

to  show  plainly  enough  the  existence  of  the  two  classes  of  material, 
the  unstratified  and  stratified.  The  unstratified  condition  character- 
izes always  the  moraine-like  heaps  of  limestone  pebbles,  and  is  in 
general  the  condition  of  the  materials  occurring  on  high  land,  and  ail 
along  the  Kettle  Range,  where,  however,  there  is  often  visible,  in  the 
sand,  a  rude  sort  of  bedding,  not  due  to  aqueous  action,  but  indicat- 
ing merely  a  gradual  growth  of  the  deposits.  The  knobby  hills, 
when  not  formed  of  limestone  pebbles,  are  often  made  up  of  layers  of 
sand  conforming  roughly  to  the  outlines  of  the  hills. 

Stratified  drift  is  to  be  seen  in  the  valleys  of  streams,  as  also  in 
many  not  now  occupied  by  streams.  A  few  instances  will  serve  to 
give  an  idea  of  what  is  a  general  truth.  About  a  mile  east  of  the' 
Wisconsin,  on  the  side  of  the  road  from  the  village  of  Knowlton, 
Marathon  county,  to  the  railroad  bridge,  finely  stratified  sand  and 
gravel  may  be  seen,  at  an  elevation  of  over  50  feet  above  the  river. 
The  pebbles  are  all  small,  much  rounded,  and  consist  predominatingly 
of  granite,  with  some  diorite,  quartz,  etc.,  and  no  limestone.  At 
Montello,  Marquette  county,  in  the  immediate  vicinity  of  the  Fox 
river,  flowing  wells  are  obtained  from  what  appears  to  be  strati- 
fied drift.  The  wells  are  50  to  90  feet  deep,  and  pass  through  a 
series  of  layers  of  sand,  gravel,  and  clay,  the  gravel  layers  at  differ- 
ent horizons  yielding  waten  A  number  of  railroad  cuttings  in  the 
vicinity  of  Madison,  and  to  the  southward  along  the  Catfish  valley, 
show  finely  stratified  drift,  one  of  the  best  points  being  at  Stoughton 
depot,  where  a  bank  25  feet  high  shows  very  regular  layers,  three 
to  four  inches  thick,  of  alternating  sand  and  gravel.  On  the  opposite 
Bide  of  the  Catfish,  at  a  lower  level,  the  following  alternation  occurs: 

Feel..    Inches. 

Soil 1 

Fine  gravel 4 

Cross-laminated  sand 4 

Fine  gravel 1          6 

Cross-laminated  sand 3 

Horizontally  laminated  sand 2         2 

White  brick  clay  to  river  level 15 

30          6 


THE  GLACIAL  DRIFT.  625 

Of  the  total  amount  of  the  drift  materials,  it  is  difficult  to  make 
a  satisfactory  estimate,  since  the  thickness  is  so  very  variable.  The 
greatest  amount  of  material  appears  to  be  in  the  region  of  the  Kettle 
Range,  and  especially  in  that  part  of  it  that  occupies  Waushara  and 
the  adjoining  counties.  Wells  in  the  town  of  Oasis,  Waushara  county, 
are  sunk  140  to  150  feet,  without  striking  rock.  The  drift  hills  of  the 
Devil's  Lake  gorge,  described  a  short  distance  back,  are  fully  200  feet 
thick,  and  may  reach  300.  The  drift  hill  on  the  University  grounds, 
Madison,  where  the  President's  house  stands,  is  107  feet  thick  to  the 
lake  level,  122  feet  to  rock.  The  Artesian  well  at  the  Capitol  Park, 
Madison,  is  180  feet  in  drift.  But  the  distinctly  stratified  drift  has 
often  also  a  considerable  thickness.  It  is  frequently  the  case  that  in 
valleys,  wells  sunk  close  to  the  rocky  side  hills  will  pass  through  50  to 
100  feet  of  stratified  gravel,  sand  and  clay.  Nearly  all  the  valleys  have 
their  rock  bottoms  far  below  their  present  surfaces,  whilst  there  are 
even  evidences  of  entirely  obliterated  valleys.  On  the  high  prairie 
of  Arlington,  which  is  nearly  everywhere  underlaid,  at  a  shallow 
depth,  by  the  Lower  Magnesian,  wells  sunk  within  a  few  rods  of  a 
ledge  of  St.  Peters  sandstone,  on  the  S.  E.  qr.,  Sec.  28,  pass  through 
over  100  feet  of  loose  materials.  Even  on  the  summit  of  the  divid- 
ing ridge  between  Black  and  Yellow  rivers,  apparently  stratified  drift 
has  a  thickness  of  over  100  feet.  In  all  of  the  drift-bearing  region, 
wells  commonly  pass  through  10  to  15  feet  of  drift-before  striking 
rock,  and  it  is  probably  far  within  the  truth  to  say  that  the  drift 
materials  are  equal  to  a  layer  50  to  60  feet  thick,  spread  over  the 
whole  drift-bearing  area. 

Three  kinds  of  evidence  are  available  with  regard  to  the  directions 
of  the  glacial  movement:  the  courses  of  the  strise  and  grooves  on 
the  underlying  rocks;  the  directions  of  the  lines  of  glacial  erosion; 
•and  the  directions  of  travel  of  erratics  of  known  origin. 

The  rocks  underlying  the  drift  quite  often  show  polishing, 
since,  and  grooves,  but  these  markings  have  not  remained  over  a 
large  portion  of  the  region,  either  on  account  of  the  exceedingly 
friable  nature  of  the  rock  on  which  they  have  been  made,  or,  if  the 
rock  be  limestone,  because  this  has  suffered  from  the  dissolving  action 
of  carbonated  water.  Moreover,  over  great  areas,  the  drift  conceals 
the  rock  basement.  The  markings  observed  are  most  commonly  on 
limestone,  which  is  frequently  planed  and  scratched  in  a  beautiful 
manner.  One  observation  only  has  been  made  on  sandstone,  and  this 
where  the  sandstone  was  unusually  hard.  The  only  Archaean  rocks 
on  which  the  markings  have  been  observed,  are  those  of  some  of  the 
isolated  areas  within  the  region  of  the  Potsdam  sandstone.  In  the 
Wis.  SUB.  — 40, 


626 


GEOLOGY  OF  CENTRAL  WISCONSIN. 


main  Archaean  region  of  the  district,  no  marked  evidence  of  glacia- 
tion  has  been  observed.  The  following  is  a  tabulation  of  the  obser- 
vations made: 

DIRECTIONS,  ETC.,  OF  GLACIAL  STRIDE  AND  FURROWS. 


o 

H 

MS 

S 

T. 

R. 

County. 

Directions  l 

Kind  of  Rock. 

Remarks. 

1 
2 

0 

4 

5 
6 

7 
8 

9 

10 

11 
12 

13 

14 
15 

sw 

NW 
NW 

NW 

NW 
SE 
NE 
SE 

NE 

NW 

NW 
NE 

SE 
SE 

NE 

11 
35 

14 

17 

21 

14 
15 

2:; 

2 

26 

•2-") 

2(5 

a 

i 

2 

5 
6 
8 

7 
7 

X 

8 
10 

11 

1-2 
12 

ia 

10 

13 

17 

12E 
12  E 

HE 

1.0  E 

9E 

8E 
8E 
8E 

6E 

7E 

7E 

8E 

12  E 
12  E 
HE 

Dane  

S.  35°  E. 
S.    5°W. 
S.  19°  W. 

S.  47°  W. 

S.  57°  W. 
S.  73°  W. 

s.srw. 

West. 
S.  65°  W. 

S.  85°  W. 

S.  50°  W. 
S.  85°  W. 

S.47.5°W. 
S.  63°  W. 
S.  68°  W. 

Trenton  Limestone 
Buff  Limestone  .  .  . 
Buff  Limestone.  .  . 

Buff  Limestone.  .  . 

Lower  Magnesian  . 
Lower  Magnesian  . 
Lower  Magnesian  . 
Lower  Magnesian  . 

Potsdam  sandstone 

Archaean  Quartzite 

Lower  Magnesian. 
Archaean  Quartzite 

Lower  Magnesian  . 
Lower  Magnesian 
Quartz-porphyry..  . 

Striations,  1  set  only. 
Striations,  1  set  only. 
Striations  .  Fainter 
lines    crossing    at 
small  angles. 
Striations.  Fainter 
strife  S.  40°  W. 
Striations,  1  set  only. 
Striations,  1  set  only. 
Striations,  1  set  only. 
Striations.  Fainter 
lines  S.  85°  W. 
Grooves  very  mark- 
edly parallel,  on  the 
"stossed"  end  of  a 
ridge. 
Grooves,    and     fine 
striations,  with  glas- 
sy polished  surface. 
Striations. 
Furrows   1'  6"  wide, 
l"-2"  deep;  striations 
in  same  direction. 
Striations. 
Striations,  1  set  only. 
Striations,  very  close, 
parallel,   with    pol- 
ished surface. 

Dane  .... 

Dane  

Dane  

Dane    

Dane  

Dane  

Columbia.  .  . 

Sauk  

Sauk  

Columbia  .  . 

Columbia  .  . 
Columbia  .  . 
Green  Lake 

The  linear  topography,  seen  in  lines  of  marsh,  in  the  directions  of 
streams,  valleys,  narrow  ridges,  and  lakes,  and  in  the  outlines  of  the 
areas  of  the  geological  formations,  has  been  described  before,  as  char- 
acterizing especially  the  region  of  Dane  and  Columbia  counties;  and 
the  bearings  of  these  lines  have  been  shown  to  coincide  with  the  bear- 
ings of  the  glacial  striae.  A  very  brief  examination  of  the  table  just 
given,  together  with  Plates  XXYI  and  XXYI  A  of  this  volume,  and 
the  Atlas  Plates  of  Areas  D  and  E  will  serve  to  show  the  following 
interesting  facts.  Beginning  on  the  southeast,  in  the  towns  of  Albion 
and  Pleasant  Springs,  and  following  a  curving  course  northwestward 
to  the  country  about  Lodi  in  Columbia  county,  we  find  the  glacial 
striae  and  the  linear  formation  outlines,  stream,  lake,  and  marsh  direc- 
tions, etc.,  undergoing  a  gradual  but  steady  change  from  a  nearly  due 
south  direction  to  one  as  nearly  due  west,  and  we  find  this  westerly 
direction  continued  further  northward  into  the  country  of -the  Baraboo 

i  True  bearings. 


THE  GLACIAL  DRIFT.  627 

ranges.  Moreover,  in  this  change  of  direction  a  constant  position  is 
maintained  at  right  angles  to  the  curving  course  of  the  Kettle  Range. 
The  southeast  bearing  observed  in  Albion  is  an  exception  to  this  state- 
ment, but  this  direction  is  evidently  merely  a  local  one,  since  in  the 
country  immediately  east,  as  I  am  informed  by  Prof.  Chamberlin,  a 
constant  direction  to  the  south  or  a  little  west  of  south  is  observed. 
Other  exceptions  appear  in  two  bearings  observed  in  the  country 
about  Baraboo,  but  these  are  from  places  in  the  valley  between  the 
two  quartzite  ranges,  and  are  evidently  due,  in  some  way,  to  their  in- 
fluence. In  going  northward  through  the  eastern  parts  of  Columbia 
and  Dane  counties,  though  some  increase  in  westing  is  seen,  the  gen- 
eral directions  are  more  nearly  southwest.  The  outline  of  an  area  of 
Trenton  limestone  that  occurs  in  the  adjoining  corners  of  Dane,  Co- 
lumbia and  Dodge  counties  has  been  given  in  Fig.  54.  North  of 
Columbia  county  the  linear  topography  continues  into  Green  Lake 
county,  but  further  west  is  not  marked,  nor  are  stride  often  to  be  ob- 
served. 

In  considering  the  origin  and  directions  of  travel  of  the  erratics 
and  pebbles  of  the  drift,  we  notice  at  once  two  classes  of  these  mate- 
rials, those  that  have  been  carried  but  short  distances  comparatively, 
and  whose  exact  place  of  origin  may  often  be  ascertained;  and  those 
that  have  traveled  all  the  way  from  the  Lake  Superior  country,  and 
whose  homes  can  generally  be  only  roughly  guessed  at.  It  is  from 
the  first  class  of  bowlders  that  we  can  get  our  best  ideas  of  the  direc- 
tions of  the  drift  movement,  not  only  because  of  the  certainty  of  their 
places  of  origin,  but  because  they  have  probably  moved  in  more  direct 
lines  than  those  that  have  come  from  great  distances.  The  following 
are  a  few  facts  in  regard  to  the  first  class  of  erratics.  In  the  eastern 
sections  of  the  town  of  Deerfield,  T.  7,  R.  12  E.,  Dane  county,  are 
many  bowlders  of  a  bluish-gray,  flinty  quartzite,  associated  with 
others  of  a  coarse  quartzite  conglomerate,  both  having  evidently  come 
from  the  mounds  of  Archaean  quartzite  that  rise  through  the  St. 
Peters  sandstone  on  Sees.  34,  35  and  36  of  the  town  of  Portland,  T. 
9,  R.  13  E.,  Dodge  connty.  The  distance  traveled  is  from  9  to  14 
miles,  and  the  direction  of  travel  S.  25°- 30°  W.,  coinciding  closely 
with  the  directions  of  the  topographical  lines.  On  the  top  of  the  hill 
just  west  of  the  depot  at  Lodi,  Columbia  county,  S.  E..qr.  of  the  !N".  "W. 
qr.  of  Sec.  27,  T.  10,  R.  8  E.,  is  a  bowlder  some  eight  feet  high,  of  hard, 
brownish  sandstone,  having  a  vitrified  or  quartzitic  weathered  crust. 
Four  to  six  miles  due  east,  on  top  of  the  high  prairie  of  Arlington, 
are  five  small  patches  of  St.  Peters  sandstone,  the  rock  of  which  has 
characters  exactly  resembling  those  of  the  bowlder  at  Lodi.  Midway 


628  GEOLOGY  OF  CENTRAL  WISCONSIN. 

between  the  bowlder  and  its  parent  rock,  on  top  of  Kingsley's  bluff, 
near  the  southeast  corner  of  Sec.  23,  the  Lower  Magnesian  is  observed 
polished  and  striated  in  a  due  west  direction.  Several  of  the  valleys 
of  southern  Lodi  coincide  with  this  direction.  It  has  been  stated  as 
a  peculiar  fact  that  bowlders  of  the  quartzite  that  make  up  the  Bnra- 
boo  ranges  are  not  found,  except  sparingly,  to  any  distance  south  of 
these  ranges,  although  of  large  size  and  abundant  on  both  flanks  of 
the  main  range,  and  even  on  its  higher  portions,  as  also  in  the  Devil's 
Lake  gorge,  and  in  the  valley  between  the  two  ranges.  The  explana- 
tion evidently  lies  in  the  fact  -that  the  east  and  west  trend  of  the 
quartzite  blufi's  has  coincided  with  the  direction  of  the  drift  move- 
ment, which  is  proved  to  have  been  nearly  due  west  by  the  bearings 
of  the  grooves  and  strice  observed.  The  little  southing  that  appears 
in  these  bearings  would  not  carry  the  bowlders  any  distance  south 
before  reaching  the  eastern  limit  of  the  driftless  region.  Bowlders 
of  dark  colored  quartz-porphyry  are  found  along  the  road  between 
Montello  and  Kingston,  Marquette  county,  having  traveled  4  to  5 
miles  a  little  south  of  east  from  the  large  outcrops  on  Sees.  2  and  3, 
T.  15,  K.  11  E.  In  the  eastern  part  of  the  town  of  Marion,  T.  18,  K. 
11  E.,  Waushara  county,  are  several  mounds  of  granite,  and  in  the 
country  for  several  miles  to  the  west  and  south  of  west,  bowlders  of 
the  same  rock  are  abundant.  One  of  these,  of  extraordinarily  great 
size,  and  already  mentioned  as  occurring  on  the  S.  E.  qr.  of  Sec.  16, 
has  traveled  in  a  direction  of  about  W.  10°  S.,  three  miles  from  the 
outcrop  on  the  east  line  of  Sec.  12.  A  number  of  angular  bowlders 
of  Lower  Magnesian  limestone  on  the  S.  E.  qr.,  Sec.  13,  T.  17,  R.  7 
E.,  Adams  county,  have  been  carried  in  a  similar  direction  from  the 
isolated  limestone  bluffs  on  Sees.  5  and  7,  T.  17,  R.  8  E.,  Marquetto 
county.  A  large  bowlder,  30.5  feet  in  circumference,  of  very  coarse 
granite,  with  large  surfaces  of  brilliant  felspar,  rests  on  top  of  tho 
hill  at  Waupaca,  Waupaca  county,  having  been  brought  eight  miles 
from  a  mound-like  outcrop  of  the  same  rock  on  Sec.  32,  T.  23,  R.  12 
E.,  in  a  direction  of  about  S.  60°  "W. 

But  these  bowlders,  wThose  origin  is  so  near  their  present  positions, 
are  but  few  in  number,  compared  with  those  that  have  corne  from 
great  distances.  Most  of  the  latter  have  been  brought  from  points 
100  to  300  miles  to  the  north,  and  possibly  from  places  still  further 
north.  It  appears  probable  that  the  region  of  the  northern  peninsula 
of  Michigan  has  afforded  a  large  proportion  of  them,  though  it  is 
quite  possible  that  many  have  come  from  the  north  shore  of  Lake 
Superior.  The  native  copper  fragments  we  may  suppose  to  have  been 
chiefly  brought  from  Keweenaw  Point,  for  a  distance  of  300  niiles 


THE  GLACIAL  DRIFT.  629 

and  over.  The  several  kinds  of  red  porphyry  erratics  are  of  very 
doubtful  origin.  No  such  rock  occurs  in  the  Huronian  or  Lauren- 
tian  of  North  Wisconsin  or  Michigan,  nor  am  I  aware  that  any  oc- 
curs in  the  Copper  series  of  Lake  Superior,  except  in  the  state  of 
conglomerate  pebbles,  which  have  evidently  been  derived  from  an 
older  series.  The  limestone  pebbles  of  the  drift  have  come  from  all 
the  Silurian  limestones  of  eastern  Wisconsin,  the  Galena  and  Niag- 
ara formations  having  furnished  the  larger  part.  These  formations 
extend  in  continuous  belts  from  the  south  to  the  north  line  of  the 
state,  so  that  it  is  not  often  possible  to  say  in  what  direction  the  peb- 
bles have  come. 

The  origin  of  the  sand  and  clay  of  the  drift  may  be  considered 
in  the  same  connection,  though  not  affording  more  than  a  general 
idea  as  to  the  direction  of  the  drift  movement.  The  great  prepon- 
derance of  sand  over  the  other  drift  materials,  in  much  of  Central 
Wisconsin,  is  without  doubt  to  be  attributed  to  the  great  surface 
spread  of  the  friable  Potsdam  sandstone  in  the  region  over  which  the 
drift  has  passed.  Sand  is,  however,  also  found  forming  most  of  the 
drift  even  far  north  in  the  Archaean  district,  where  it  is  sometimes  in 
quantity  sufficient  to  produce  sand  barrens.  This  fact  may  be  regarded 
as  proving  a  much  greater  surface  extent  north  and  east  in  the 
Archaean  area  of  the  sandstone  formation  in  preglacial  times.  The 
clay  has  come  partly,  perhaps,  from  the  limestone  formations,  and 
partly  from  the  kaolinization  of  felspathic  erratics,  but  its  principal 
source  would  seem  to  have  been  the  previously  kaolinized  granites 
and  gneisses  of  the  Archaean  region.  It  is  well  known  that  in  all 
southern  regions  where  the  drift  phenomena  are  unknown,  as  for  in- 
stance along  the  Blue  Ridge  from  Virginia  to  Alabama,  and  in  Bra- 
zil, the  felspathic  crystalline  rocks  are  found  rotted  to  great  depths. 
Hunt  has  drawn  attention  to  the  fact  that  in  the  region  of  the  Blue 
Ridcje  this  ceases  to  be  the  case  north  of  the  southern  limit  of  the 

O  v 

glacial  drift,  whose  deposits  lie  upon  the  hard,  unaltered,  and  often 
polished  rock  surface,  and  has  inferred  the  removal  of  the  softened 
rock  by  the  glacial  forces.  In  that  small  portion  of  the  Archaean 
region  of  Wisconsin,  in  which  the  drift  is  insignificant  or  wanting 
entirely  —  as  along  the  valley  of  the  Wisconsin  south  of  Stevens 
Point,  arid  along  Black  river  south  of  the  crossing  of  the  Green  Bay 
road — decomposed  and  kaolinized  gneiss  and  granite  occur.  Over 
the  rest  of  the  Archaean  region,  on  the  contrary,  the  drift  rests  directly 
upon  the  unchanged  rock. 

No  fossils  of  any  kind  have  ever  come  to  my  attention  as  occurring 
in  the  drift  deposits  of  Central  Wisconsin. 


630  GEOLOGY  OF  CENTRAL  WISCONSIN. 

The  economic  contents  of  the  drift  are  of  considerable  importance. 
In  many  regions  of  the  state  where  other  limestones  are  either  absent 
or  yield  only  an  inferior  lime,  the  pebbles  of  the  drift  are  profitably 
burnt.  They  yield  often  an  excellent  white  lime,  as,  for  instance,  at 
several  points  on  the  Baraboo  ranges,  and  in  the  sand  region  of  Mar- 
quette  and  Waushara  counties.  The  sand  and  gravel  of  the  drift  are 
everywhere  put  to  use  for  the  ordinary  purposes.  The  gravel  is  occa- 
sionally transported  far  into  the  drif tless  region  for  railroad  ballast  • 
ing.  The  stratified  clays  of  the  drift  are  everywhere  used  for  brick- 
making,  yielding  often,  as  at  Stoughton  and  Oregon,  in  Dane  county, 
a  cream-colored  brick  fully  equal  to  the  '*  Milwaukee  brick." 

The  facts  given  in  the  foregoing  pages  will  warrant  a  few  briefly 
stated  theoretical  conclusions : 

(1)  The  drift  of  Central  Wisconsin  is  true  glacier  drift)  as  is 
well  shown  by  facts  similar  to  those  that  are  appealed  to  as  proof  of 
the  same  thing  in  other  glaciated  regions,  viz.:  the  unstratified  nature 
of  the  drift  materials,  except  in  stream  valleys;  the  frequent  moraine- 
like  drift  hills  and  ridges;  the  absence  of  fossils,  marine  or  otherwise; 
the  abundance  of  well  rounded,  scratched,  and  polished  bowlders;  the 
existence  of  a  "till"  with  its  striated  pebbles ;  the  polished,  striated 
and  grooved  condition  of  the  underlying  rock  surface;    the  linear  and 
parallel  erosion  outlines;  and  the  entire  lack  of  any  evidence  of  such  a 
submergence  of  the  region  as  would  be  necessary  for  the  working  of 
any  other  distributor  of  loose  materials  than  a  glacier.     Moreover,  in 
this  special  case,  there  is  positive  evidence  that  no  such  submergence 
ever  did  take  place.     This  evidence  is  found  in  the  sharply  defined 
character  and  position  of  the  drift  limit,  which  pays  no  attention  what- 
ever to  the  topography  of  the  country  it  traverses,  having  the  higher 
ground  now  on  one  side,  now  on  the  other,  and  crossing  the  highest 
ridges  and  lowest  valleys  indifferently.     Only  a  glacier  could  have 
ceased  its  action  along  such  a  line.     Had  the  drift  materials  been 
spread  by  floating  bergs,  the  sea  in  which  these  were  borne  would 
never  have  ceased  along  such  an  abrupt  line,  and,  moreover,  any  sea 
which  was  deep  enough  to  have  floated  icebergs  over  the  higher  por- 
tions of  the  Baraboo  ranges  would  have  carried  them  westward  unin- 
terruptedly to  the  Mississippi  river. 

(2)  The  Kettle  Range  of  Central  Wisconsin  is  a  continuous  ter- 
minal and  lateral  moraine.     The  mere  fact  of  the  existence  of  such 
a  distinct  and  continuous  belt  of  unstratified  and  moraine-like  drift, 
which,  in  much  of  its  course,  lies  along  the  edge  of  the  driftless 
area,  or,  in  other  words,  along  the  line  on  which  the  western  foot  of 
a  glacier  must  long  have  stood,  would  go  far  towards  proving  the 


THE  GLACIAL  DRIFT.  631 

truth  of  this  proposition,  of  which,  however,  a  complete  demonstra- 
tion appears  to  be  at  hand.  In  all  the  country  just  inside  of  the 
Kettle  Range,  we  find  that  glacial  striae,  lines  of  glacial  erosion,  and 
lines  of  travel  of  erratics,  all  preserve  a  position  at  right  angles  to  the 
course  of  the  range,  although  that  course  veers  in  the  southern  part 
of  the  district  from  west  to  north.  East  of  the  Central  Wisconsin 
district,  as  previously  stated,  the  Kettle  Range  extends  eastward  and 
northeastward  to  the  dividing  ridge  between  the  valley  of  Lake  Mich- 
igan and  the  valley  in  which  lie  Green  Bay,  Lake  Winnebago  and  the 
head  waters  of  Rock  river,  and  along  this  ridge  northward  into 
Green  Bay  peninsula.  All  along  this  part  of  its  course,  Prof. 
Chamberlin  has  found  the  glacial  striaa  pointing  east  of  south,  and 
towards  the  Kettle  Range,  whilst  along  the  middle  of  the  Green  Bay 
valley,  he  finds  the  strise  directions  parallel  to  the  main  axis  of  the 
valley,  or  a  little  west  of  south.  On  the  west  side  of  this  great  valley, 
and  along  the  eastern  border  of  the  Central  Wisconsin  district,  the 
strise  trend  about  southwest,  whilst  still  further  west  they  gradually 
trend  further  to  the  west,  becoming  at  last  nearly  due  west,  or  at 
right  angles  to  the  western  Kettle  Range. 

We  have  then  a  most  beautiful  proof  that  at  one  time  the  Green 
Bay  valley  was  occupied  by  a  glacier,  which  was  not  merely  part  of  a 
universal  ice  sheet,  but  a  distinctly  separate  tongue  from  the  great 
northern  mass.  The  end  of  this  glacier  was  long  in  northern  Rock 
county,  its  eastern  foot  on  the  east  Wisconsin  divide,  and  its  western 
on  the  summit  of  the  divide  between  the  Fox  and  Wisconsin  river 
systems,  as  far  south  as  southern  Adams  county,  after  which  it  crossed 
into  the  valley  of  the  Wisconsin,  arid  from  that  into  the  headwaters 
of  the  Catfish  branch  of  Rock  river,  in  the  Dane  county  region. 
Whilst  the  main  movement  of  the  glacier  coincides  in  direction  with 
the  valley  which  it  followed,  it  spread  out  on  both  sides  in  fan-shape, 
creating  immense  lateral  moraines.  Peculiar  circumstances  caused 
the  restriction  of  the  eastern  moraine  to  a  narrow  area,  whilst  that  on 
the  west,  having  no  such  restriction,  spread  out  over  a  considerable 
width  of  country,  the  breadth  of  the  moraine  reaching  in  Waushara 
county  as  much  as  25  miles.  Of  course  this  width  of  moraine  must 
have  been  due  to  the  alternate  advance  and  retreat  of  the  glacier  foot. 
Such  an  advance  and  retreat  appears  moreover  to  be  recorded  in  the 
long  lines  of  narrow  sinuous  ridges,  each  marking  perhaps  the  posi- 
tion of  the  glacier  foot,  or  a  portion  of  it,  during  a  certain  length  of 
time.  The  intersecting  of  these  winding  ridges,  which  have  no  par- 
allelism at  all  with  one  another,  appears  to  me  to  have  been  the  main 
cause  of  the  formation  of  the  kettle  depressions.  Col.  Whittlesey1 
1  Smithsonian  Contributions  to  Knowledge. 


632  GEOLOGY    OF   CENTRAL  WISCONSIN. 

lias  supposed  that  these  owe  their  origin  to  the  melting  of  ice  masses 
included  within  the  moraine  materials,  and  this  may  possibly  be  true 
with  regard  to  the  more  regularly  circular  kettles. 

The  thickness  of  the  great  glacier  we  can  only  conjecture.  It  is 
easy  to  see,  however,  that  it  was  at  least  a  thousand  feet,  for  it  was 
able  to  accommodate  itself  to  variations  in  altitude  of  many  hundred 
feet.  Morainic  drift  occurs  on  the  summit  of  the  Baraboo  ranges 
over  900  feet  above  Lake  Michigan,  and  on  the  immediately  adjacent 
low  ground  700  feet  below. 

(3)  The  Driftless  Region  of  Wisconsin  owes  its  existence,  not  to 
superior  altitude,  but  to  the  fact  that  the  glaciers  were  deflected 
fro-m  it  l>y  the  influence  of  the  valleys  of  Green  Bay  and  Lake 
Superior.  Some  writers 1  have  thrown  out  the  idea  that  the  drif tless 
area  is  one  of  present  great  altitude  compared  with  the  regions  around 
it,  and  that  by  virtue  of  this  altitude  during  the  Glacial  period  it 
caused  a  splitting  of  the  general  ice  sheet,  itself  escaping  glaciation. 
This  idea  may  have  arisen  from  the  fact  that  in  the  southern  part  of 
the  area  the  district  known  as  the  "  Lead  Region  "  has  a  considerable 
elevation;  but  the  facts  heretofore  given  have  shown  that  in  reality 
the  driftless  area  is  for  the  most  part  lower  than  the  drift-covered 
country  immediately  around;  the  greatest  development,  for  instance, 
of  the  western  lateral  moraine  of  the  glacier  of  the  Green  Bay  valley, 
having  been  on  the  very  crown  of  the  watershed  between  the  Lake 
Michigan  and  Mississippi  river  slopes,  whilst  the  driftless  region  is 
altogether  on  the  last  named  slope.  Moreover,  to  the  north,  towards 
Lake  Superior,  and  to  the  west,  in  Minnesota,  the  whole  country 
covered  with  drift  materials  lies  at  a  much  greater  altitude.  J.  D. 
Whitney,  in  his  report  on  the  lead  region  of  "Wisconsin,  favors  the 
idea  that  the  driftless  district  stood,  during  the  glacial  times,  at  a 
much  greater  relative  altitude  than  now,  and  so  escaped  glaciation. 
But  it  is  evident  that  in  order  that  this  could  have  been  the  case, 
either  (1)  a  break  or  bend  in  the  strata  must  have  taken  place  along 
the  line  of  junction  between  driftless  and  drift-bearing  regions;  or 
else  (2)  the  driftless  region  has  since  received  a  relatively  vastly 
greater  amount  of  denudation  than  the  drift-bearing.  That  no  break 
or  bend  ever  took  place  along  the  line  indicated  is  abundantly  proven 
by  the  present  perfect  continuity  of  the  strata  on  both  sides  of  the 
line,  the  whole  region  of  Central  Wisconsin  being-  in  fact  one  in 
which  faults  of  any  kind  are  things  absolutely  unknown.  That  no 
sensible  denudation  has  taken  place  in  Wisconsin  since  the  Glacial 
times,  in  either  drift  bearing  or  driftless  areas,  is  as  well  proven  by  the 

1  See  Geological  Survey  of  Ohio,  Vol.  II. 


THE  GLACIAL  DRIFT.  633 

intimate  connection  with  one  another  of  the  systems  of  erosion  of  the 
two  regions.  The  valley  of  Sugar  river,  for  instance,  with  itsbranches, 
is  throughout  its  course  worn  deeply  into  the  underlying  rocks;  on 
its  east  side  it  contains  morainic  drift,  proving  that  it  was  worn  out 
before  the  Glacial  period,  whilst  on  the  west  it  extends  into  the  drift- 
less  regions. 

O 

We  are  thus  compelled  to  believe  that  during  the  Glacial  period 
the  region  destitute  of  drift  had  the  same  altitude  relatively  to  the 
surrounding  country  as  at  present.  Before  the  Glacial  period  por- 
tions of  the  drift-bearing  region  may  indeed  have  been  somewhat 
higher,  for  in  it  a  considerable  amount  of  material  must  have  been 
removed  from  one  place  to  another,  by  the  glacial  forces.  The  only 
satisfactory  explanation  remaining  then  for  the  existence  of  the  drift- 
less  region  is  the  one  I  have  proposed.  We  have  already  seen  that 
the  extent  of  this  region  to  the  eastward  was  marked  out  by  the  west- 
ern foot  of  the  glacier  which  followed  the  valley  of  Green  Bay.  That 
it  was  not  invaded  from  the  north  is  evidently  due  to  the  fact  that  the 
glacier  or  glaciers  of  that  region  were  deflected  to  the  westward  by  the 
influence  of  the  valley  of  Lake  Superior.  The  details  of  the  movement 
for  this  northern  country  have  not  been  worked  out,  but  it  is  well  known 
that  what  is  probably  the  most  remarkable  and  best  preserved  devel  • 
opment  of  morainic  drift  in  the  United  States  exists  on  the  water- 
shed south  of  La,ke  Superior.  Here  the  drift  attains  a  very  great 
thickness,  and  the  kettle  depressions  and  small  lakes  without  outlet 
are  even  more  numerous  and  characteristic  than  in  other  parts  of  the 
state.  The  watershed  proper  lies  some  30-40  miles  south  of  the  lake, 
and  800  to  1200  feet  above  it,  but  the  morainic  drift  extends  25  to  50 
miles  further  southward.  On  the  east  side  of  the  state  the  drift  of 
Lake  Superior  merges  with  that  of  central  and  eastern  Wisconsin, 
whilst  west  of  the  western  moraine  of  the  Green  Bay  glacier,  it  dies 
out  somewhat  gradually,  until  125  to  150  miles  south  of  the  lake  the 
the  drift  limit  is  reached.  Much  of  the  country  25  to  75  miles  north 
of  the  driftless  region,  though  showing  numerous  erratics,  is  quite 
without  any  marked  signs  of  glaciation;  as,  for  instance,  along  the 
valley  of  the  Wisconsin  from  Grand  Rapids  north  to  Wausau.  Fur- 
ther \vest  the  drift  extends  more  to  the  southward.  The  course  of  the 
Lake  Superior  glaciers  conveyed  them  further  and  further  southward 
as  they  moved  westward. 

Future  investigations  will  imdoubtedly  bring  out  a  close  connec- 
tion between  the  structure  of  the  Lake  Superior  valley  and  the  glacial 
movements  south  of  it.  Even  the  facts  now  at  hand  seem  to  point 
toward  some  interesting  conclusions.  Projecting  from  the  south 


634  GEOLOGY  OF  CENTRAL  WISCONSIN. 

shore  of  Lake  Superior,  we  find  two  great  promontories,  Keweenavr 
Point,  and  the  Bayfield  Peninsula.  Both  of  these  projections  have  a 
course  somewhat  transverse  to  the  general  trend  of  the  lake,  bearing 
some  30°  south  of  west.  Both  have  high  central  ridges  or  backbones, 
which  rise  1,000  to  1,500  feet  above  the  adjacent  lake,  and  are  made 
up  of  bedded  igneous  rocks,  sandstones,  and  conglomerates  of  theCop- 
per  Series.  Both  of  these  ridges  continue  far  westward  on  the  main- 
land, having  between  them  a  valley,  partly  occupied  by  the  lake, 
which  is  a  true  synclinal  trough,  the  rocks  of  the  two  ridges  dipping 
towards  one  another,  North  of  the  Bayfield  Peninsula,  and  again 
south  of  Keweenaw  Point,  we  find  two  other  valleys  running  in  from 
the  lake  shore  in  the  same  direction.  In  all  probability  each  one  of 
these  valleys  has  given  direction  to  a  glacier  tongue.  An  inspection 
of  a  good  map  of  the  northern  part  of  Wisconsin,  Minnesota  and 
Michigan  will  serve  to  show  that  the  almost  innumerable  small  lakes1 
of  these  regions  are  concentrated  into  three  main  groups,  each  group 
corresponding  to  a  great  development  of  morainic  drift,  and  lying  in 
the  line  of  one  of  the  three  valleys  just  indicated.  I  suppose  that 
each  of  the  lake  groups  is  a  moraine  of  the  glacier  which  occupied 
the  valley  in  whose  line  it  lies.  The  main  ice  sheet  coming  from 
the  north  met,  in  the  great  trough  of  Lake  Superior,  over  2,000  feet  in 
depth,  an  obstacle  which  it  was  never  able  to  entirely  overcome,  and 
so  reached  further  southward  in  small  tongues  composed  perhaps  of 
only  the  upper  portions  of  the  ice.  These  tongues  being  deflected 
westward  by  the  rock  structure  of  the  country,  and  having  their  force 
mainly  spent  on  climbing  over  the  watershed,  left  the  region  further 
south  untouched.  The  eastern  part  of  the  Lake  Superior  trough  is 
not  nearly  so  deep  as  the  western,  and  the  divide  between  Lake  Su- 
perior and  the  two  lakes  south  of  it  never  attains  any  great  altitude, 
so  that  here  the  ice  mass,  having  at  the  same  time  perhaps  a  greater 
force  on  account  of  its  nearness  to  the  head  of  the  ice  movement  on 
the  Laurentian  highlands  of  Canada,  was  able  to  extend  southward 
on  a  large  scale,  producing  the  glaciers  of  the  Green  Bay  valley  and 
of  Lake  Michigan. 

Although  quite  crude  in  its  details,  I  am  convinced  that  the  main 
points  of  the  explanation  thus  offered  for  the  -existence  of  the  drift- 
less  region  in  the  northwest  will  prove  to  be  correct.  To  obtain  a  full 
elucidation  of  the  subject,  much  must  yet  be  done  in  the  way  of  in- 
vestigation, not  only  in  Wisconsin,  but  over  all  of  Minnesota  and  the 
states  south,  in  order  that  the  details  of  the  ice  movement  for  the 
whole  northwest  may  be  fully  understood. 

1  Far  more  numerous  in  reality  than  shown  on  the  best  maps. 


LACUSTRINE  CLAYS  — BOG  IRON  ORES.          635 

(4.)  The  stratified  drift  of  the  valleys  owes  its  structure  and  distri- 
bution to  the  u'</t<;i'  of  the  swollen  streams  and  lakes  that  marked  the 
time  of  melting  of  the  glaciers. 

(5.)  The  depth  below  the  present  surfaces  of  the  rock  valleys  ap- 
pears to  indicate  a  greater  altitude  of  this  part  of  the  continent,  du- 
ring the  Glacial  period,  than  at  the  present  time. 

LACUSTRINE  CLAYS. 

Extending  inland  from  Lakes  Michigan  and  Superior  for  many- 
miles,  and  reaching  elevations  of  several  hundred  feet  above  the  lakes, 
are  stratified  beds  of  loose  material,  chiefly  marly  claj'S,  with  more 
or  less  sand,  some  gravel  and  a  few  bowlders.  These  are  proved  to 
be,  with  but  little  doubt,  of  lacustrine  origin,  by  the  manner  in  which 
they  follow  the  shores  of  the  lakes,  and  they  register  a  depression  of 
several  hundred  feet,  corresponding  to  the  period  subsequent  to  the 
melting  of  the  glaciers,  when  all  the  lakes  and  streams  of  the  north- 
ern part  of  the  United  States  were  greatly  expanded  beyond  their 
present  limits,  and  the  whole  northern  part  of  the  continent  stood  at 
a  lower  level. 

In  the  Central  Wisconsin  district  the  lacustrine  clays  have  only  a 
small  development,  most  of  the  district  being  either  too  high  to  have 
been  reached  by  the  lake  depositions,  or  else  lying  behind  the  divid- 
ing ridges.  The  eastern  towns  of  Waushara  county,  however,  are 
underlaid  by  a  considerable  thickness  of  red  clay  belonging  to  this 
formation.  The  surface  elevation  of  the  country  here  is  160  to  200 
feet  above  Lake  Michigan,  and  the  clays  80  to  100  feet  and  over  in 
depth,  as  shown  by  numerous  Artesian  well  borings  that  yield  a  flow 
of  water  which  is  obtained  from  seams  of  gravel  at  different  horizons 
in  the  clay.  The  clay  of  eastern  Waushara  county  is  part  of  a  large 
clay  area  that  extends  up  the  Green  Bay  valley  from  Lake  Michigan. 

BOG  IRON  ORES. 

The  most  recent  formations  of  the  Central  Wisconsin  district  are 
the  marsh  deposits  of  peat  and  bog  iron  ore.  The  latter  is  fdund  on 
a  small  scale  underlying  the  peat  of  many  marshes,  and  also  occur- 
ring at  points  not  now  marshes,  but  still  showing  signs  of  a  marsh 
origin.  The  large  marshes  of  Juneau,  Wood  and  Portage  counties 
have  yielded  the  best  indications  of  the  existence  of  good  bog  ore, 
although  the  points  at  wrhich  any  quantity  can  be  seen  are  few  in 
number. 

At  Necedali,  Juneau  county,  immediately  south  of  an  isolated 
hill  of  Arehoean  quartzite,  is  a  tongue  of  the  great  marsh  that 


636  GEOLOGY  OF  CENTRAL  WISCONSIN. 

spreads  widely  over  northwestern  Juneau  county  and  into  the  adjoin- 
ing counties  of  Jackson  and  "Wood.  Underneath  the  peat  of  this 
marsh  tongue,  and  along  the  banks  of  a  dry  run  east  of  the  marsh, 
bog  ore  occurs  in  some  quantity.  The  best  ore  is  found  on  the  S.  E. 
qr.  of  Sec.  24,  T.  18,  E.  3  E.,  on  land  belonging  to  Mr.  J.  T.  Kings- 
ton, where  it  lies  at  about  &  feet  below  the  surface  of  the  marsh,  be- 
ing covered  by  peat  and  peaty  marsh  mud.  It  is  seen  in  the  bottom 
of  a  ditch  for  some  40  rods,  and  can  be  raised  by  the  crowbar  in  large 
firm  blocks.  These  are  very  porous,  but  between  the  pores  show  a 
dark  brown,  very  hard,  fibrous,  silky-lustred  limonite.  Immediately 
over  the  hard  ore,  in  places,  is  a  sand  or  shot  ore,  composed  of  rolled 
grains  of  limonite.  The  thickness  is  reported  at  2^  feet.  The  fol- 
lowing analysis  shows  the  composition  of  a  sample  (1356)  averaged 
from  a  considerable  quantity:  silica,  8.52;  alumina,  3.77;  iron  perox- 
ide, 71.40;  manganese  oxide,  0.27;  lime,  0.58;  magnesia,  trace;  phos- 
phoric acid,  0.21;  sulphur,  0.02;  organic  matter,  1.62;  water, 
13.46  =  99.85:  metallic  iron,  49.98.  Following  the  stream  south- 
ward into  the  N.  E.  qr.  of  Sec.  25,  the  ore  grows  much  leaner,  being 
mingled  with  sand  (1356^).  The  same  sandy  ore  is  seen  along  the 
side  of  a  dry  run  on  the  1ST.  W.  qr.  of  Sec.  30,  T.  18,  E.  4  E.,  an  aver- 
age sample  yielding  only  16.09  per  cent,  of  metallic  iron.  Mr. 
Kingston's  ore  is  certainly  an  excellent  one,  and  the  marsh  is  well 
worthy  of  further  investigation. 

At  Point  Bass,  "Wood  county,  on  the  west  bank  of  the  Wisconsin 
river,  near  the  center  of  Sec.  10,  T.  21,  E.  5  E.,  on  land  belonging  to 
the  Hon.  Moses  M.  Strong,  a  porous  bedded  limonite  is  exposed  in  the 
river  bank,  15  feet  above  the  water.  The  exposure  extends  along  for 
some  50  feet,  and  appears  to  be  some  8  feet  in  thickness,  the  upper 
3  feet  being  a  porous  but  quite  pure  ore,  containing  some  50  per 
cent,  of  metallic  iron.  Two  hundred  feet  down  stream  a  cutting  into 
the  river  bank  shows  that  the  ore  does  not  continue  in  that  direction. 
At  several  points  on  the  east  bank  of  the  Wisconsin,  north  of 
Grand  Rapids,  on  Sec.  4,  T.  22,  E.  6  E.,  and  Sec.  34,  T.  23,  E.  6  E., 
small  openings  show  ore  just  like  that  described.  At  one  of  these 
points,  on  Mr.  McGrath's  land,  the  ore  is  seen  with  a  thickness  of  20 
inches,  very  evenly  and  thinly  bedded,  and  extending  over  an  area  of 
about  75  feet  square.  The  following  analysis,  made  by  Mr.  Oliver 
Matthews,  a  student  of  the  Metallurgical  Department  of  the  State 
University,  shows  the  composition  of  an  averaged  sample:  silica, 
4.81;  alumina,  1.00;  iron  peroxide,  73.23;  lime,  0.11;  magnesia, 
0.25;  sulphuric  acid,  0.07;  phosphoric  acid,  0.10;  organic  matter, 
5.88;  water,  14.24=99.69:  metallic  iron,  51.26. 


APPENDIX  — MICROSCOPIC  L1THOLOGY.  '  637 


APPENDIX. 


MICROSCOPIC  LITHOLOGY, 


BY  CHARLES  E.  WRIGHT. 


[NOTE.  —  The  following  descriptions  are  of  a  small  number  of  crystalline  rocks  selected  from  th-i 
large  mass  of  material  on  hand,  as  most  difficult  to  determine,  or  as  having  a  special  importance. 
The  numbers  are  the  same  as  given  in  the  body  of  the  report,  and  the  original  specimens  will  bo 
found  in  the  survey  collections,  when  distributed.  A  few  of  Mr.  Wright's  descriptions  have  been 
made  use  of  in  the  foregoing  pages,  but  the  descriptions  of  crystalline  rocks  there  given  are 
nearly  always  wholly  my  own.  It  is  a  matter  of  regret  that  the  funds  were  not  available  for  micro- 
scopic examination  of  a  full  suite  of  the  Central  Wisconsin  rocks.  R.  D.  I.] 

501.  Silicious  Hornblende-Schist.  HURONIAN?  Black  river,  Jackson  county, 
north  line  Sec.  %4,  T.  21^  R.  4  W.  Light-greenish-black;  very  fine-grained;  crystalline 
texture;  eonchoidal  fracture;  bard  and  compact.  With  the  lens,  minute  grains  of  silica 
are  plainly  visible,  but  the  ingredient  minerals  cannot  be  distinguished.  Under  the  mi- 
croscope, in  the  polarized  light,  a  thin  section  of  the  rock  presents  a  very  pretty  field, 
and  is  composed  of  small  fragments  of  aniphibole,  minute  grains  of  quartz,  and  a  few 
scattered  leaves  of  chlorite.  From  the  structure  it  is  evident  that  the  amphibole  f  ormed 
after  the  quartz,  since  the  fonner  encloses  grains  of  the  latter. 

757.  Granite.    HURONIAN?     Village  of  Montelln,  Marquette  county,  S.  W.  qr. 
Sec.  9,  T.  15,  R.  10  E.    Pale  flesh-color,  dotted  with  a  few  dark  patches  of  mica.    The 
facets  of  felspar  are  easily  recognized.    Traversing  the  specimen  is  a  thin,  light-green- 
ish seam  of  what  appears  to  be  epidote.     Under  the  microscope,  in  the  polarized  light, 
the  coarse  fragments  of  orthoclase  apparently  constitute  more  than  one-half  the  en- 
tire section.     An  occasional  twin  crystal  of  felspar  after  the  Carlsbad  form  may  bo 
seen.    The  grams  of  quartz  are  mostly  very  small  and  angular,  and  are  frequently 
enclosed  within  the  felspar.    With  a  power  of  500  diameters  are  visible,  in  the  quartz, 
fluid  inclusions;  the  absence,  however,  of  any  glass  or  stone-filled  cavities  will  no  doubt 
refer  the  rock  to  a  metamorphic  origin. 

758.  Argillo-chloritic  Schist.  HURONIAK?  Village  of  Montello,  Marquette  County, 
S.  W.  qr.  Sec.  9,  T.  15,  R.  10  E.    Grayish-green;  fine-grained  texture;  partially  decom- 
posed; cleaves  readily  into  irregular  plates;  in  the  joints  it  is  often  ocherous;  under  the 
microscope  the  pale  greenish  leaves  of  chlorite  are  plainly  visible;  also  minute  grains  of 
silica  and  a  few  scales  of  hematite. 


638  GEOLOGY  OF  CENTRAL  WISCONSIN. 

766.  Granite.  HUROXIAN?  Near  Spring  Lake,  Waushara  county,  N.  E.qr.  Sec. 
27,  T.  IS,  R.  11  E.  Similar  to  757  from  Montello.  The  felspar  is  more  or  less  decom- 
posed; but  this  is  probably  local  or  accidental. 

859  1-2.  Hornblende  Schist.  LAURENTIAN.  Grand  Rapids  of  Hie  Wisconsin, 
Wood  count//,  S.  W.  qr.  Sec.  8,  T.  22,  R.  6  E.  Bright  greenish- black  sprinkled  with  gray; 
fine-grained,  highly  crystalline  texture;  conchoidal  fracture;  the  fresh  surface  having  a 
raspy  feel ;  several  specks  of  iron  pyrites  are  strewn  along  the  joints ;  under  the  microscope 
can  be  easily  recognized  the  amphibole,  and  considerable  orthoclase  felspar;  also  angular 
grains  of  quartz  and  several  fluid  inclusions,  or  small  liquid-filled  cavities.  The  speci- 
men resembles  the  hornblende- schist  of  the  Marquette  iron  district. 

897.  Hornblende  Rock.    LAURENTIAX.    Little  Bull  Falls,  Marathon  county,  Sec. 
29,  T.  27,  R.  7  E.    Dark  grayish- green;  medium  to  fine-grained,  crystalline  texture;  un- 
even fracture  and  somewhat  jointed.    The  mineral  ingredieuts  can  not  well  be  distin- 
guished with  the  lens.     Under  the  microscope,  however,  the  amphibole,  and  plain  and 
striated  fragments  of  felspar,  are  easily  recognized;  also,  a  little  chlorite,  and  a  few 
grains  of  quartz. 

898.  Syenite.    LAURENTIAN.    Little  Bull  Falls,  Marathon  county,  Sec.  29,  T.  27, 
R.  7  E.    Greyish-white,  spotted  with  greenish-black;  coarse-grained  texture;  the  amphi- 
bole and  felspar  are  plainly  visible  to  the  naked  eye.     Under  the  microscope  the  felspar 
appears  to  be  somewhat  altered,  and  a  few  of  the  crystals  are  striated.     An  occasional 
fragment  of  quartz  may  be  seen;  also  a  little  chlorite.    The  former  contains  fluid  in- 
clusions. 

898  a.  Hornblende  Rock.  LAURENTIAN.  Little  Bull  Falls,  Marathon  county,  Sec. 
29,  T.  27,  R.  7  E.  Greenish-black,  mottled  with  grayish- white;  medium  to  coarse- 
grained; uneven  fracture;  the  felspar  and  amphibole  are  plainly  visible.  It  resembles 
very  much  a  diorite.  Under  the  microscope,  the  essential  minerals  are  easily  recognized. 
The  felspar,  owing  to  the  partial  decomposition,  presents  a  milky  texture,  which  fre- 
quently renders  it  nearly  opaque.  The  grains  of  quartz,  however,  are  clear  and  limpid. 
The  specimen,  no  doubt,  is  a  coarser  variety  of  897. 

902.  Silicions  Chloritic  Schist  (provisional).  LAURENTIAN.  Little  Bull  Falls, 
Marathon  county,  Sec.  29,  T.  27,  R,  7  E.  Very  dark  greenish-gray,  and  slightly 
tinged  with  bluish-black;  weathers  to  a  light  drab;  fine-grained  texture  and  schistose 
structure.  Under  the  microscope,  the  section  appears  composed  of  chlorite,  small 
grains  of  silica,  brownish  leaves  of  mica,  and  a  few  fragments  of  amphibole. 

905.  Chloritic  Hornblende  Rock.  LAURENT-IAN.  Little  Bull  Falls,  Marathon 
county,  Sec.  29,  T.  27,  R.  7  E.  Greenish-black;  aphanitic  texture;  very  jointed  and  ap- 
parently schistose;  weathers  to  a  dirty  drab.  Under  the  microscope  can  be  seen  the  am- 
phibole and  quartz.  The  felspar  is  very  much  altered,  but  may  be  recognized  by  a  mo- 
ment's careful  observation.  Considerable  chlorite  is  contained,  also  an  occasional  scale  of 
mica.  It  is  possible  that  this  rock  is  a  less  altered  variety  of  902,  and  therefore  passing 
into  a  silicious  chloritic  schist. 

907.  Syenitic  Granite.    LAURENTIAN.    Big  Bull  Falls,  Marathon  county,  Sec. 
26,  T.  29,  R.  7  E.    Pinkish,  speckled  with  greenish-black;   medium-grained  texture; 
rough,  uneven  fracture.    The  felspar  is  easily  recognized.    The  amphibole  and  black 
mica  are  scarcely  to  be  distinguished  from  each  other,  even  with  a  strong  lens.     Under 
the  microscope  this  similarity  still  exists,  but  the  position  of  the  optical  bisectrix  to  the 
principal  crystallographic  axis  in  the  hornblende  readily  separates  it  from  the  mica. 
The  former,  however,  is  in  excess  of  the  latter.    The  felspars  are  mostly  twinned,  after 
the  Carlsbad  form;  some  of  them  appear,  in  the  polarized  light,  to  be  irregularly  band- 
ed, which  is  probably  due  to  an  unequal  decomposition.    Numerous  angular  grains  of 
quartz  are  present.    The  rock  is  evidently  metamorphic. 

908.  Syenite.    LAURENTIAN.    Bic/  Bull  Falls,  Marathon  county,  Sec.  26,  T.  29, 


APPENDIX— MICROSCOPIC  LITHOLOGY.  (839 

R.7E.  Gray,  thickly  speckled  with  black;  fine  to  medium-grained;  rough,  uneven 
fracture;  the  felspar  and  hornblende  are  plainly  visible  to  the  naked  eye.  Under  the 
microscope,  each  of  the  above  minerals  is  easily  recognized.  The  felspar  fragments 
are  chiefly  plain,  though  a  few  of  them  are  beautifully  striated  in  one  direction.  Very 
little  quartz  is  contained. 

910.  Syenite.  LATJRENTIAN.  Big  Bull  Falls,  Marathon  county,  Sec.  35,  T.  29,  R. 
7  E.  Same  as  908,  but  coarser  grained,  and  some  of  the  grains  of  quartz  contain  cavi- 
ties filled  with  a  salt  solution,  out  of  which  have  crystallized  small,  transparent  cubes  of 
salt.  The  small  bubble  and  crystals  are  easily  distinguished  from  each  other,  even 
when  the  comers  of  the  cube  are  rounded,  by  the  difference  of  their  refractive  indices. 
Scarcely  any  motion  is  perceptible  in  the  bubbles,  even  when  heated  to  130°  C. 

915.  Silicions  Hornblende-Schist.  LAURENTIAX.  West  bank  of  Wisconsin 
river,  north  line  Sec.  26,  T.  29,  B.  7  E.  Grayish-black;  very  fine-grained,  arenaceous 
texture;  jointed  and  irregular  fracture.  Under  the  microscope,  in  the  polarized  light, 
the  section  appears  composed  of  a  silicious  base,  interspersed  with  fragments  of  am- 
phibole,  felspar,  and  dark  colored  mica.  The  felspar  is  of  two  varieties,  one  in  small 
striated  fragments,  and  the  other  in  large  plain  ones,  which  are  very  much  altered,  fre- 
quently so  much  so  that  only  an  indistinct  outline  remains. 

932.  Chloro-Silicious-Schist  (provisional).  LAURENTIAN.  East  Bank  Wis- 
consin river,  S.  W.  (jr.  Sec.  1,  T.  29,  R.  7  E.  Grayish-green;  aphanitic  texture; 
conchoidal  fracture;  slightly  banded.  Under  the  microscope  the  greenish  chloritic 
base  is  interspersed  with  small  angular  grains  of  felspar  and  silica.  An  occasional  patch 
of  ealcite  may  be  recognized. 

9 32  a.  Very  Silicious  Marble1  (provisional.)  LAURENTIAN.  East  bank  Wis- 
consin river,  S.  W.  qr.  Sec.  1,  T.  29,  R.  7  E.  Grayish-green;  aphanitic  texture; 
conchoidal  fracture;  slightly  banded.  A  fragment  thrown  into  acid  effervesces  briskly, 
for  a  time,  without  disintegrating.  Under  the  microscope  it  presents  an  indefinite 
fringy  base,  strewn  with  small  crystals  of  felspar,  grains  of  quartz,  and  greenish  leaves 
of  chlorite. 

948.  Chloro-Silicious-Schist  (provisional).  LAURENTIAN.  Falls  of  Big  Rib  riter, 
Marathon  county,  N.  E.  qr.  Sec.  28,  T.  29,  R.  5  E.  Resembles  932.  Under  the 
microscope  the  base  of  the  rock  is  composed  largely  of  decomposed  crystals  of  felspar; 
scattered  in  this  are  numerous  fragments  of  amphibole  and  leaves  of  chlorite.  The  rock 
is  apparently  an  altered  hornblende-schist. 

948a.  Chloro-Silicious-Scuist  (provisional).  Same  place  as  948,  to  which  it  is 
closely  similar. 

950.  Syenite.  LAURENTIAN.  Falls  of  Biff  Rib  river,  Marathon  county,  N.  E.  qr. 
Sec.  28,  T.  29,  R.  5  E.  Light- pinkish-gray,  mixed  with  dark-gray  and  black;  medi- 
um to  coarse-grained,  indefinite  texture.  A  few  crystal- facets  of  felspar  may  be  recog- 
nized, but  they  are  mostly  too  much  altered  to  have  preserved  their  cleavage.  This 
altered  condition  is  very  apparent  under  the  microscope,  where  the  section  appears 
thickly  strewn  with  indistinct  outlines  of  the  altered  crystals,  though  some  are  quite 
fresh.  The  amplibole  is  also  somewhat  changed.  A  few  angular  grains  of  quartz  are 
present,  and  they  show  liquid  inclusions. 

952.  Granite.  LAUREXTIAX.  Falls  of  the  Big  Rib  riter,  Marathon  county,  N.  E. 
qr.  Sec.  28,  T.  29,  R.  5  E.  Grayish-white,  spotted  with  dark-green;  medium-grained. 
With  the  loupe,  small,  glassy  grains  of  quartz  may  .be  recognized.  The  felspar  is  so 
much  decomposed  that  it  shows  but  little  signs  of  cleavage.  Under  the  microscope  the 
crystals  of  felspar  are  grayish  and  indistinctly  outlined.  A  greenish  chlorite  is  contained, 

i  This  rock  is  merely  a  phase  of  the  preceding  one  (932)  moat  specimens  of  which  show  no 
effervescence  with  acid.  it.  D.  I. 


640  GEOLOGY  OF  CENTRAL  WISCONSIN. 

which  is  very  much  altered.  The  grains  of  quartz  appear  angular,  and  contain  nuraer' 
ous  fluid  inclusions. 

953.  Chloritic  Schist  (provisional).  LAUREXTIAX.  Falls  of  Big  Rib  river,  N. 
E.  q>:  Sec.  28,  T.  29,  R.  5.  E.,  Marathon  county.  Light  and  dark-green;  talcose  or 
chloritic  texture;  warped  schistose  structure.  Hardness  about  4.  Under  the  microscope 
a  section  of  the  specimen  appears  to  consist  largely  of  altered  crystal  fragments  of  fel- 
spar, and  grains  of  quartz,  scattered  in  a  greenish  chloritic  base.  The  rock  is  probably  a 
syenitic  and  hornblende  schist  ash. 

958.  Talco-Mica-Schist.  ARCHAEAN.  Cutting  on  the  W.  V.  R.  R.,  three 
miles  north  of  Junction  City,  Sec.  24,  T.  25,  R.  6  E.  Light  drab;  talcose  texture  on 
lamination  planes  and  arenaceous  across  the  grain;  cleaves  readily  into  irregular  finely- 
ribbed  plates ;  somewhat  altered,  and  emits  a  strong  clay  odor  when  moistened.  Under 
the  microscope  the  light  scales  of  talc  are  hardly  distinguishable  from  those  of  mica,  but 
the  dark  ones  of  the  latter  are  more  easily  recognized.  The  section  is  composed  largely 
of  small  angular  grains  of  silica.  The  argillaceous  odor  is  due  to  the  numerous  de- 
composed fragments  of  felspar. 

961.  Calcareous  Mica-Schist.    ARCHAEAN.     Cutting  on  W.  V.  R.  R.,  two  and  a 
half  miles  north   of  Junction  City.      Sec.  26,    T.   25,  R.    6   E.,    Portage    county. 
Dark-green;  fine-grained  texture.     A  fracture  in  the  direction  of  the  cleavage  glistens 
with  bright,  dark  greenish-black  scales  of  mica.     A  lump  thrown  into  acid  effervesces 
briskly,  leaving  a  friable  mass.   Under  the  microscope  the  crystals  of  calcite  are  striated 
showing  then:  usual  proneness  to  twin.     The  angular  grains  of  quartz  and  leaves  of 
mica  (biolite)  are  readily  distinguished,  also  opaque  crystal  cubes  of  pyrites.    The  separ- 
ate mineral  ingredients  are  arranged  in  bands  or  layers. 

962.  Mica-Schist.    ARCHAEAN.    From  cutting  on  W.  V.  R.  R.,  one  and  a  half 
miles  north  from  Junction  City,  Sec.  35,  T.  25,  R.  6  E.,  Portage  county.    Light  drab; 
fine-grained,  arenaceous  texture  across  the  lamination;  slightly  shimmering  along  the 
schist  planes.    The  minute  scales  of  mica  are  hardly  recognizable  to  the  naked  eye. 
Under  the  microscope,  in  the  polarized  light,  a  section  of  the  specimen  appears  brightly 
colored  with  angular  grains  of  silica.   The  base  of  the  rock  presents  a  dirty  appearance, 
and  scattered  in  it  are  the  brownish  leaves  of  mica  and  a  few  altered  crystal  fragments 
of  felspar. 

963.  Hornblende-Schist.    ARCH/EAST.    From  a  cutting  on  the  W.  V.  R.  R.,  % 
mile  north  of  Junction  City,  Sec.  35,  T.  25,  R.  6  E.,  Portage  county.     Dark-green.     It 
is  somewhat  altered  and  has  a  dirty  lock.    The  single  mineral  ingredients  can  barely 
be  recognized  with  the  naked  eye,  but  under  the  microscope  are  plainly  visible  the 
amphibole,  quartz  and  mica,  also  a  little  chlorite. 

964.  Hornblende-Schist.    ARCHAEAN.    From  a  cutting  on  the  W.  V.  R.  R.,  7 1-2 
miles  south  from  Junction  City,  north  part,  of   T.  23,  R.  6  E.,  Wood  county.     Dark 
grayish-green;    fine-grained,     crystalline-texture;     schistose    structure    and    jointed; 
weathers  to  a  drab.     Under  the  microscope  it  appears  to  consist  mostly  of  amphi- 
bole.   Several  small  grains  of  quartz  are  contained,  also  a  little  chlorite. 

968.  Chloritic  Rock.  ARCH.EAN.  From  east  side  of  Wisconsin  river,  5  miles 
south  of  Mosime.  T.  26,  R.7E.,  Marathon  county.  Grayish-green;  aphanitic  text- 
ture;  very  jointed  and  apparently  schistose.  Under  the  microscope  the  base  of  the  sec- 
tion presents  a  moss-like  microcrystalline  structure,  and  scattered  through  it  are  highly 
altered  crystals  of  felspar,  wlu'ch  are  usually  very  indistinct,  only  the  faint  outUr.es  re- 
maining. With  a  power  of  500  diameters  the  small  pale-greenish  leaves  of  chlorite  are 
visible,  also  numerous  minute  particles  of  magnetite. 

970.  Quartz-Porphyry.  ARCHAEAN.  From  the  bed  of  Yellow  river,  3  miles  north 
of  Dexterville,  Sec.  3,  T.  22,  R.  3  E.,  Wood  county.  Light  pea-green;  massive;  resem- 
bles some  of  the  quartzites.  Several  crystal-facets  of  felspar  may  be  seen,  also  an  occa- 


APPENDIX  — MICROSCOPIC  LITHOLOGY.  641 

sional  small  quartz  crystal.  Under  the  microscope  a  section  of  the  specimen  appears 
composed  chiefly  of  felspar,  with  a  few  crystals  of  quartz  scattered  through  it.  The 
quartz  resembles  that  contained  in  igneous  rocks,  since  some  of  the  crystals  enclose,  ap- 
parently, portions  of  "the  matrix.  Their  richness,  however,  in  fluid  cavities,  would  no 
doubt  preclude  such  a  supposition.  The  felspar  is  somewhat  altered  and  presents  fre- 
quently a  fringy  texture.  A  few  spherulites  of  felspar  so  common  to  quartz-porphyries 
may  be  recognized. 

992.  Felspathic-Schist  (provisional).  ARCH^AN.  Cutting  on  W.  V.  R.  R.,  3.7 
miles  south  of  Knowlton,  Sec.  12,  T.  25,  R.  6  E.,  Portage  county.  Grayish-drab;  fine- 
grained, indefinite  texture.  A  few  minute  crystal-facets  are  visible;  emits  a  strong  clay 
odor  when  breathed  upon.  Under  the  microscope  the  rock  appears  very  felspathic.  and 
some  of  the  crystals  are  beautifully  banded.  Numerous  small  angular  grains  of  quartz 
are  contained,  also  brownish  leaves  of  mica,  and  a  fibrous  mineral  resembling  talc. 

997.  Actinnlite-Schist.  AKCH^AN.  Cutting  on  W.  V.  R.  R.,  3.7  miles  south  of 
Knowlton,  Sec.  12,  T.  25,  R.  6  E.,  Portage  county.  Light-green,  medium-grained,, 
crystalline  texture.  The  cleavage  facets  of  the  actinolite  are  easily  recognized.  It  is 
somewhat  decomposed.  Under  the  microscope  the  actinolite  presents  a  reticulated 
structure;  a  little  quartz,  felspar  and  chlorite  are  contained. 

1003.  Diorite.    ARCH^AN.    From  bed  of  Black  river,  Mormon  Ripple,  Sec.  3,  T. 
22,  R.  3  W.,  Jackson  county.     Light-and-dark-green;  weathers  to  a  light-drab;  me- 
dium-grained texture,  with  coarse  crystals  of  amphibole  strewn  through  the  mass. 
Under  the  microscope  the  principal  mineral  ingredients  appear  to  be  amphibole  and 
felspar;  the  latter  is  of  two  kinds,  plain  and  striated.     An  occasional  crystal  fragment 
resembling  augite  is  contained,  also  a  little  chlorite. 

1004.  Quartzite.    ARCHAEAN.    From  bed  of  Black  river,  Mormon  Ripple,  Sec.  3, 
T.  22,  R.  3  W.,   Jackson  county.    Light  reddish-gray,  with  streaks  of  dark-green; 
quartzose,  vitreous  texture.     Under  the  microscope  appears,  in  addition  to  the  quartz,  a 
considerable  number  of  slightly  altered  crystals  of  orthoclase  and  greenish  leaves  of 
mica  or  possibly  chlorite,  though  they  are  apparently  the  former,  since  they  are  strongly 
diehroitic. 

1005.  Felspathic  Quartzite,  or  Granite.    ARCHJEAN.    From  bed  of  Black  river, 
at  Mormon  Ripple,  Sec.  3,  T.  22,  R.  3  W.,  Jackson  county.    Flesh  color;  medium- 
grained  texture.     On  a  fresh  fracture  may  be  seen  numerous  bright  cleavage  facets  of 
felspar.     Under  the  microscope  the  felspar  and  quartz  appear  to  be  about  efjually  di- 
vided.    The  former  are  mostly  plain  crystals,  and  the  latter  enclose  numerous  fluid 
cavities. 

1007.  Micaceous  Schist.     ARCHAEAN.    From  the  bed  of  Black  river,  at  Mormon 
Ripple,  Sec.  3,  T.  22,  R.  3  W.,  Jackson  county.  Drab;  fine-grained,  arenaceous  texture; 
somewhat  decomposed  and  emits  a  strong  clay  odor  when  moistened.     Under  the  mi- 
croscope a  section  of  the  specimen  appears  to  consist  largely  of  altered  brownish  frag- 
ments, resembling  mica.     Scattered  in  the  base  are  numerous  small  angular  grains  of 
silica. 

1008.  Granite.    ARCH/BAN.     From  bed  of  Black  river,    at  Black   River  Falls, 
Sec.  15,  T.  21,  R.  4  W.,  Jackson  county.    Flesh-color,  spotted  with  dark-green;  medium- 
grained  texture.    The  crystal-facets  of  felspar  and  grains  of  quartz  are  plainly  visible 
to  the  naked  eye.     Under  the  microscope,  the  felspar  appears  to  be  more  largely  con- 
tained than  the  quartz.    But  little  mica  is  present. 

1412.  Quartz-Porphyry.  HURONIAN?  Pine  Bluff,  N.  W.  qr.  of  the  N.  E.  qr. 
of  Sec.  2,  T.  11,  R.  11  E.,  Green  Lake  county.  Grayish-white;  fine-grained  texture, 
and  porphyritic  with  glassy  crystals  of  felspar,  which  resemble  sanadin.  Under  the 
microscope,  the  specimen  seems  to  be  an  intimate  mixture  of  felspar  and  quartz.  Some 
of  the  felspar  crystals  have  an  appearance  as  if,  after  they  were  formed,  they  had  been 
Wis.  Sun.  —  41 


GEOLOGY  OF  CENTRAL  WISCONSIN, 

partially  dissolved,  or  replaced  in  part  by  crystalized  silica;  the  latter  presenting  in  the 
polarized  light  colored  patches  which  have  frequently  their  crystallographic  axes  all 
lying  in  the  same  direction.  On  the  other  hand,  many  of  the  quartz  grains  enclose  crys- 
tals of  felspar,  but  these  may  be  instances  where  the  felspathic  material  has  been 
almost  entirely  replaced  by  the  silica.  The  quartz  resembles  vein  quartz  and  contains  a 
few  fluid  inclusions. 

1430.  Quartz-Porphyry.  HTTROXIAN?  From  head  of  Lake  Buffalo,  N.  E.  qr. 
of  Sec.  8,  T.  14,  R.  9.  E.,  Marquette  county.  Dark  reddish-brown;  porphyritic  texture. 
The  cleavage  facets  of  the  felspar  are  the  only  mineral  ingredients  that  can  be  recog- 
nized by  the  naked  eye.  With  the  microscope,  the  base  presents  a  semi-granular  moss- 
like  texture,  in  which  are  strewn  a  few  crystals  of  orthoclase  and  quartz,  also  numerous 
small  crystal  grains  of  magnetite.  To  the  latter  is  due  the  dark  color  of  the  rock. 


PL  ATE,  XXVI 


VIEW  OF  BLUFF  OF  GALENA  LIMESTONE, 
Near  Cassville  oil  the  Mississippi. 


PAET  IT. 


GEOLOGY  AND  TOPOGRAPHY 


OF 


THE  LEAD  REGION. 


BY  MOSES  STRONG. 


GEOLOGY  AND  TOPOGRAPHY- 


OP 


THE  LEAD  REGION, 


CHAPTEE  I. 
INTRODUCTORY   AND   HISTORICAL.  ' 

Survey  of  1873.  In  accordance  with  my  instructions  received 
from  the  late  Dr.  I.  A.  Lapham,  in  May,  1873,  to  make  a  survey  of 
two  lines,  with  sections  of  the  strata;  one  north  and  south,  and  the 
other  east  and  west,  crossing  at  or  near  Mineral  Point,  work  was  com- 
menced on  the  5th  of  June,  1873,  at  Scales  Mound,  111.,  as  being 
near  the  southern  boundary  of  the  Lead  region. 

The  territory  examined  during  the  year  1873  is  as  follows:  Town 
29  JN".,  ranges  2  and  3  E.,  in  the  state  of  Illinois;  towns  1  to  13  inclusive, 
in  ranges  2  and  3  E.,  in  the  state  of  Wisconsin;  towns  4  and  5,  on 
ranges  1  to  6  "W.,  to  the  Mississippi  river;  towns  4  and  5,  on  ranges 
1,  2,  3,  4  and  5  E. ;  towns  6,  7,  8  and  9,  on  ranges  5  and  6  E.,  to  the 
Wisconsin  river,  being  in  all  an  area  of  about  50  townships. 

Explorations  were  chiefly  confined  to  the  territory  already  men- 
tioned; departures  were,  however,  occasionally  made  for  the  purpose 
of  visiting  localities  of  geological  interest  or  mineralogical  import- 
ance. In  order  to  complete  the  survey  of  so  large  a  tract  of  country, 
it  was  necessary  to  traverse  an  average  area  of  twelve  square  miles 
per  day.  Such  an  amount  precluded  anything  more  than  a  careful 
examination  of  the  more  important  localities,  and  a  general  inspection 
of  the  rest. 

The  advantages  of  this  plan  of  operations  were  numerous,  but 
chiefly  these:  that  by  the  examination  of  a  tract  of  country  twelve 
miles  in  width,  passing  through  the  center  of  Grant,  Iowa  and  La 
Fayette  counties,  a  large  and  comprehensive  view  of  the  entire  Lead 
region  was  secured,  so  far  as  its  general  features  were  concerned;  the 


646     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

details  of  which,  belonging  to  each  separate  locality,  could  be  more 
easily  and  intelligently  obtained  in  the  progress  of  the  survey  of 
this  and  the  succeeding  year.  Further,  it  was  necessary  for  topo- 
graphical purposes  to  ascertain  the  elevation  of  numerous  points, 
which  should  be  readily  accessible  to  the  various  parts  of  the  region, 
as  will  be  more  fully  explained  under  the  subject  of  Barometrical 
Observations. 

The  greater  part  of  the  summer  of  1873  was  devoted  to  these  pur- 
poses, and  spent  within  the  confines  of  the  Lead  region,  with  the 
exception  of  the  latter  part  of  July,  and  two  \veeks  in  August,  which 
were  passed  in  the  counties  of  Sauk  and  Richland,  in  the  examination 
of  the  Potsdam  and  Lower  Magnesian  formations,  and  the  iron  ore 
deposits  incidental  thereto. 

Survey  of  1874.  The  territory  examined  in  that  year  was  as  fol- 
lows: 

Towns  1,  2,  3,  6,  7,  8,    - 
"     2,3,6,7,        -        - 
"     2,3,6,7,    -        - 
"3,6, 

"     1,  2,  3,  6,  7,  8,    - 
"     1,  2,  3,  4, 
"     1,2,3,4,    - 

The  townships  here  enumerated  comprise  the  northern  and  south- 
ern parts  of  Grant  county,  the  eastern  and  western  parts  of  La  Fayette 
county,  the  western  part  of  Iowa  county,  and  that  part  of  it  which  is 
drained  by  Mill  creek,  the  whole  of  Green  county,  the  western  part 
of  Bichland  county,  and  some  parts  of  Yernon,  Monroe  and  Jackson 
counties. 

The  field  work  was  commenced  on  the  14th  of  May,  1874,  nearly 
three  weeks  earlier  than  in  1873.  The  total  area  examined  is  equal 
to  sixty-six  full  townships,  being  an  increase  of  sixteen  over  the  pre- 
vious year. 

The  first  examinations  were  made  in  the  vicinity  of  Cassville,  pro- 
ceeding eastward  from  there  to  the  eastern  boundary  of  Green  county, 
and  visiting  successively  all  the  mining  districts  and  individual 
mines,  of  which  a  full  report  will  be  found  in  chapter  IY.  After 
examining  the  Mill  creek  district,  the  survey  next  proceeded  to  range 
two  west,  north  of  the  "Wisconsin  river,  including  the  valley  of  Knapp 
creek  and  the  upper  Kickapoo,  and  as  far  north  as  the  Green  Bay  & 
Minnesota  railroad.  Finally  returning  from  there,  the  northeastern 
part  of  Iowa,  and  the  northern  part  of  Grant  counties  were  examined, 
together  with  that  part  of  the  valley  of  the  Wisconsin  winch  lies 
south  of  the  river. 


R.  1  W. 

Towns  1,  2.  3,  6  to  22  inclusive, 

R.  2W. 

R.  3W. 

3,  6,  7,     -        -        -        - 

R.  5W. 

R.  4  W. 

1,  2,  3,  6,  7,  8,    - 

R.  1   E. 

R.  6  W. 

1,2,  3,    - 

R.  5  E. 

R.  4   E. 

1,  2,  3,  4,    - 

R.  7  E. 

R.  6   E. 

1,2,3,4,        -        -        - 

R.  8  E. 

-        - 

R.  9  E. 

INTRODUCTORY  AND  HISTORICAL.  617 

Previous  Publications  and  Surreys.  The  first  geological  survey 
embraced  the  extensive  district  lying  between  the  Missouri  river  and 
Red  river  of  the  J^orth,  and  included  the  upper  part  of  the  valley  of 
the  Mississippi  and  the  mining  districts  adjacent  to  that  river.  It 
was  undertaken  in  1834,  and  completed  in  1835,  by  the  general  gov- 
ernment, and  placed  in  charge  of  G.  W.  Featherstonhaugh. 

The  next  survey  was  also  instituted  by  the  general  government, 
and  placed  under  the  direction  of  Dr.  D.  D.  Owen,  in  the  fall  of 
1839,  and  completed  by  him  in  the  same  year;  its  object  being  to  as- 
certain the  geographical  position  of  the  Lead  region  and  its  value  as 
mineral  land.  Dr.  Owen  was  afterward  engaged  in  the  geological 
survey  of  the  Chippewa  Land  District,  during  1847-8,  of  which  he 
published  a  final  report  in  1851,  accompanied  by  a  general  geological 
map.  The  exploration  of  so  large  a  district  did  not  admit  of  a  mi- 
nute examination  of  any  particular  part:  thus,  the  space  devoted  to 
the  southwestern  part  of  the  state,  and  lying  south  of  the  Wisconsin, 
river,  is  comprised  in  about  twenty  pages  of  chapter  I. 

The  next  geological  survey  was  undertaken  under  the  auspices  of  the 
state,  in  1853,  and  placed  in  charge  of  Prof.  E.  Daniels,  who  published 
in  1854  a  pamphlet  concerning  the  Lead  region.  He  was  then  suc- 
ceeded by  Dr.  J.  G.  Percival,  who  held  the  position  of  State  Geolo- 
gist, until  his  death,  in  May,  1856.  He  published  two  reports  of 
about  100  pages  each,  which  contain  much  valuable  information,  and 
bear  evidence  of  the  careful  research  which  always  distinguished  his 
work. 

To  complete  the  survey  interrupted  by  the  death  of  Dr.  Percival, 
Profs.  James  Hall,  E.  S.  Carr  and  E.  Daniels  were  appointed;  and,  in 
1858,  Prof.  Daniels  published  a  report  of  about  60  pages,  on  the  iron 
ores  of  "Wisconsin.  This  was  succeeded  by  the  report  of  Profs.  Hall 
and  Whitney,  in  January,  1862.  This  was  by  far  the  largest  report 
that  had  been  published  concerning  the  Lead  region.  It  comprised 
about  450  pages,  of  which  300  were  devoted  to  that  district.  This 
report  was  accompanied  by  a  crevice  map  of  the  mineral  ranges,  and 
a  general  geological  map  of  the  Lead  region.  The  latter,  so  far  as  it 
was  made  from.personal  observation,  was  quite  correct;  but  it  still  left 
much  to  be  desired  in  this  department;  which  deficiencies,  it  is  be- 
lieved, have  been  supplied  by  the  present  survey. 

For  ten  years  the  Geological  survey  was  discontinued.  The  next, 
being  the  examinations  of  Rev.  John  Murrish,  of  which  he  published 
a  report  in  1872.  in  a  pamphlet  of  sixty-five  pages. 

Topographical  and  Geological  Maps  and  Sections.  A  great  deal 
of  time  has  been  devoted  to  the  construction  of  the  maps  accompanying 


618  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

the  report,  so  as  to  represent  the  topographical  features  of  the  country 
with  accuracy.  The  topographical  maps  herewith  published  embrace 
all  the  Lead  region.  They  comprise  the  country  lying  south  of 
town  six,  and  extending  from  the  Mississippi  river  eastward,  to  the 
line  between  Rock  and  Green  counties,  with  the  exception  of  town 
five  in  ranges  4,  5,  6,  7,  8  and  9  E.  The  maps  are  made  on  the  scale 
of  one  inch  to  the  mile,  and  exhibit  by  contour  lines,  fifty  feet  apart 
(vertically),  the  elevation  of  any  point  above  the  level  of  the  sea.  The 
elevation  of  any  point  not  on  these  lines  must  be  determined  by  its 
relative  distance  from  the  two  contour  lines  between  which  it  lies. 
In  addition  to  this  feature  (not  found  on  any  other  map),  a  complete 
road-map  is  presented;  also  a  map  of  the  streams  and  dry  ravines, 
many  of  the  smaller  streams  having  become  dry  since  the  original  gov- 
ernment survey  of  the  country  was  made.  Again,  from  an  inspection 
of  these  maps,  can  be  seen  the  rise  of  the  various  streams,  and  the 
height  of  the  dividing  ridges.  This  is  also  of  special  value  in  respect 
to  railroad  surveys,  when  the  amount  of  time  and  money  is  consid- 
ered, which  is  annually  spent  in  ascertaining  these  points.  It  is  be- 
leived  that  a  tolerably  correct  idea  of  the  practicability  or  impractic- 
ability of  any  contemplated  route  can  be  obtained  by  reference  to 
these  elevations,  arid  thus  a  vast  amount  of  preliminary  surveying 
may  be  dispensed  with. 

One  of  the  principal  objects  of  the  field-work  has  been  the  careful 
delineation  of  the  geology  of  all  parts  of  the  country,  and  its  correct 
representation  on  the  colored  maps  which  accompany  the  reports.  In 
addition  to  the  general  geological  maps  of  the  state  drawn  on  a  scale 
of  three  miles  to  the  inch,  the  geology  of  the  Lead  region  has  also 
been  placed  upon  the  topographical  maps.  The  effect  of  this  is  to 
show  the  dip  and  thickness  of  the  strata  and  "  the  exact  position  of 
the  mining  ground  at  each  locality."  The  great  extent  of  country 
which  has  been  examined  and  mapped,  together  with  the  time  and 
means  which  admitted  of  only  a  general  survey,  in  which  the  contour 
lines,  both  geological  and  topographical,  could  be  sketched  only  by 
the  eye,  preclude  that  accuracy  which  is  attainable  only  with  the  tran- 
sit and  level.  For  such  imperfections  and  inaccuracies  as  may  be 
found  to  exist  in  the  maps,  these  circumstances  must  be  our  apology 
and  explanation. 

The  geological  sections  accompanying  the  maps  are  chiefly  valuable 
as  showing  the  "  dip,  number,  magnitude,  order  and  relative  position 
of  the  various  strata,"  as  well  as  the  amount  of  denudation  to  which 
the  conntry  has  been  subjected.  They  are  located  as  far  as-  possible 


IFTRODUCTORY  AND  HISTORICAL.  649 

in  the  general  direction  of  the  dip,  in  order  to  show  the  structure,  ar- 
rangement and  irregularities  of  the  strata. 

Barometrical  Observations.  Considerable  time  has  been  devoted 
to  ascertaini  11%  the  relative  heights  of  different  parts  of  the  country, 

o  O  *-  *   ' 

for  the  purpose  of  ascertaining  the  amount  of  denudation,  and  pre- 
paratory to  making  geological  sections.  These  observations  con- 
sumed a  great  deal  of  time,  and  were  made  with  much  care;  the  plan 
followed  being  as  follows:  A  series  of  repeated  observations  were 
made  at  points  about  half  a  mile  apart,  from  the  Illinois  Central  rail- 
road at  Scales  Mound,  to  Calamine,  on  the  Mineral  Point  railroad,  and 
from  there  to  Mineral  Point.  A  similar  series  was  then  carried  from 
there  to  Lone  Rock,  on  the  Chicago,  Milwaukee  and  St.  Paul  railroad, 
and  from  there  to  Lavalle,  on  the  Chicago  and  Northwestern  railway. 
In  the  same  manner  a  series  was  carried  from  Mineral  Point  through 
Lancaster,  to  Glenhaven,  on  the  Mississippi  river,  and  from  Mineral 
Point  east,  to  Moscow,  and  thence  north,  over  the  Blue  Mounds,  to 
Mazomanie;  and  also  from  Moscow  to  Oregon,  on  the  Chicago  and 
Northwestern  railway.  Starting  from  these  known  elevations,  re- 
peated observations  were  taken;  and  the  mean  of  several  series  of 
elevations,  differing  but  little  from  each  other,  was  assumed  -to  be 
approximately  correct.  Then,  from  the  various  points  on  those  lines, 
series  of  lines  were  traveled  over,  embracing  observations  in  all  the 
accessible  points  in  the  Lead  region. 

The  instrument  used  was  a  three-inch  aneroid  barometer,  imported 
by  Wm.  J.  Young  &  Sons,  of  Philadelphia;  a  very  delicate  instru- 
ment, and  one  which  indicated  differences  of  elevation  with  great 
readiness  and  accuracy.  The  accuracy  and  value  of  barometrical  ob- 
servations depend  greatly  on  the  state  of  the  weather  at  the  time  they* 
are  made.  The  summer  seasons  have  been,  as  a  general  thing,  quite 
favorable  for  such  observations,  and  in  cases  where  it  was  not,  allow- 
ance has  been  made  in  computing  the  elevations.  They  may  be  con- 
sidered as  correct  within  a  few  feet.  For  the  extent  of  this  part  of 
the  work  the  reader  is  referred  to  the  topographical  maps,  which 
show  what  has  been  done  much  better  than  it  can  be  described. 

The  value  of  a  work  of  this  kind  is  incalculable.  By  means  of  the 
elevations  obtained,  we  are  readily  enabled  to  make  sections  of  any 
part  of  the  country,  in  any  direction;  showing  the  geological  position 
of  the  strata,  with  their  dip,  thickness,  and  the  amount  of  denudation 
at  any  particular  locality.  In  mining  localities  this  is  especially  val- 
uable. It  shows  the  position  of  the  strata  and  openings,  with  their 
dip;  the  elevation  of  the  neighboring  streams,  and  the  practicability 
of  drainage,  by  means  of  levels;  the  depth  to  which  shafts  must  be 


650 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


sunk  from  any  point  on  the  surface,  to  reach  any  particular  stratum. 
All  these  things,  and  many  others  of  like  nature  are  most  readily 
shown  by  sections,  and  these  sections  cannot  be  made  without  eleva- 
tions. 

For  particular  elevations  of  streams,  roads,  hills,  section  lines, 
mining  grounds,  strata,  outcrops,  etc.,  reference  is  made  to  the  maps 
accompanying  this  report.  From  them  a  few  are  selected,  of  general 
importance,  as  being  well  known  localities: 


LOCALITY. 


ELEVATIONS 
ABOVE 


The  Lake 

Sea.  Mich. 

Wyalusing *. 611  38 

Glen  Haven,  P.  0 606  28 

Cassville 608  30 

North  Andover 8:38  260 

Bloomington 905  327 

Patch  Grove 1060  498 

Mount  Hope 1076  498 

Little  Grant 828  250 

Beetown 762  184 

Potosi 782  204 

British  Hollow 865  287 

Rockyille 926  348 

Hurricane  Grove 941  363 

Lancaster,  court  house 1080  502 

Mount  Ida 1168  590 

Homer  P.  0 978  400 

Fennimore 1168  590 

Liberty  Ridge 1144  566 

Annaton 849  -  271 

Ellenboro' 689  111 

Dickeyville 9:34  356 

Jamestown,  P.  O 912  334 

Fairplay,  P.  0 798  220 

Sinsmawa  Academy 926  348 

Hazel  Green 9:38  360 

St.  Rose 994  416 

Big  Patch 817  239 

Platteville,  P.  0 &35  257 

Washburn 841  263 

New  California 989  411 

Montfort 1093  515 

Castle  Rock 847  269 

Highland,  P.  0 1161  583 

Cross  Plains  (Iowa  Co.) 1198  620 

Mifflin 868  290 

West  Platte  Mound 1272  694 

Behnont 828  250 

Elk  Grove 898  320 

Meeker  Grove 835  257 


LOCALITY. 


ELEVATIONS 
ABOVE 


The  Lake 

Sea.  Mich. 

Benton 878  300 

New  Diggings 792  214 

White  Oak  Springs 928  350 

Shullsburg,  school  house  . .  1018  440 

Linden 1078  500 

Union  Mills 798  220 

Kings  Mills 723  145 

Dodge ville,  court  house "...  1109  531 

Mineral  Point,  depot 935  357 

Calamine,  depot 812  2:34 

Darlington,  depot 802  224 

Gratiot,  depot 783  205 

Fayette 1053  475 

Adamsville 878  300 

West  Blue  Mound 1729  1151 

Blanchardville 758  180 

Wiota 996  418 

Martin 865  287 

Cadiz 859  281 

Argyle 808  230 

Jordan 858  280 

Wfflett 888  310 

Farmers  Grove 1118  540 

Bern 1078  500 

Perry 1038  460 

New  Glarus,  P.  0 968  390 

Monticello 858  280 

Monroe,  court  house 1018  410 

Clarno 935  357 

Twin  Grove 988  410 

Juda 821  243 

Sylvester 865  287 

Dayton 818  240 

Brooklyn 978  400 

Attica,  P.  0 828  250 

Albany 818  240 

Brodhead 798  220 

Oakley 918  340 


The  following  elevations  of  stations  have  been  furnished  by  the 
Chicago,  Milwaukee  and  St.  Paul  Railroad  Company,  and  were  used 
as  a  basis  of  some  of  the  barometrical  observations: 


INTRODUCTORY  AND  HISTORICAL.  651 

Elevation     Above  Lake 

above  Sea.      Michigan. 

Black  Earth 810  232 

Mazomanie 770  195 

Arena  732  154 

Spring  Green 722  144 

Lone  Rock 704  126 

"  Avoca 695  117 

Muscoda 687  109 

Boscobel 667  89 

Wauzeka 638  60 

Prairie  du  Chien 619  41 

Finally,  it  may  be  said  of  the  elevations,  that  they  are  by  far  the 
most  important  and  valuable  part  of  the  work,  inasmuch  as  they  form 
the  ground-work  of  the  whole,  and  we  are  entirely  dependent  on  them 
for  definite  results.  They  have  been  made  and  computed  with  the 
utmost  accuracy  and  care.  Lastly,  they  comprise  that  portion  of  the 
work,  which,  from  its  nature,  consumes  the  most  time,  and  makes  the 
least  outward  show. 

In  conclusion,  I  desire  to  express  my  thanks  for  the  hearty  co- 
operation which  the  survey  has  met  at  the  hands  of  the  citizens  of  the 
Lead  region,  who  have  willingly  furnished  all  desired  information 
and  statistics,  often  at  no  small  inconvenience  to  themselves. 

My  thanks  are  also  due  to  Mr.  Allan  D.  Conover,  of  Madison,  my 
assistant  during  the  year  1873;  to  Mr.  George  Haven,  of  Minneapolis, 
Minn.,  my  assistant  during  the  years  1874-1875,  who,  by  the  careful 
discharge  of  their  duties  in  the  field,  have  contributed  materially  to 
the  completeness  of  the  work. 


652  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


OHAPTEE  II. 
TOPOGKAPHY   AND   SUEFACE   GEOLOGY. 

TOPOGRAPHY. 

General  Features  of  the  Country.  Unlike  most  regions  wliicli 
nature  has  selected  for  the  reception  of  metallic  ores  and  useful  min- 
erals, the  Lead  region  bears  no  evidences  of  any  sudden  disturbances, 
or  violent  action  of  physical  forces.  The  effects  produced  by  igneous 
and  eruptive  agencies  are  wanting.  Faults  and  dislocations  of  strata 
are  nowhere  found.  The  only  irregularities  are  slight  upheavals,  or 
bending  of  the  strata  (and  these  never  of  great  extent),  producing 
changes  of  but  a  few  feet  from  the  normal  dip. 

Between  the  geological  condition  and  the  general  surface  contour 
of  the  country,  there  is  no  direct  correlation.  The  existence  of  a  hill 
or  a  valley  on  the  surface  is  not  due  to  a  subterranean  elevation  or 
depression  of  the  surface,  as  is  by  many  supposed,  and  whatever  irreg- 
ularities exist,  must  be  chiefly  attributed  to  the  milder  natural  agen- 
cies now  constantly  at  work;  such  as  running  water,  frost,  winds,  etc., 
acting  through  an  immensely  long  period  of  time. 

Drainage.  The  most  marked  and  persistent  feature  of  the  Lead 
region  is  the  long  dividing  ridge,  or  watershed,  which,  commencing 
near  Madison,  continues  almost  directly  west  to  the  Blue  Mounds,  a  dis- 
tance of  about  twenty  miles.  Here  it  takes  a  slight  bend  to  the  south- 
west for  fifteen  miles,  until  it  reaches  Dodgeville,  where  it  resumes  its 
westerly  course  until  it  terminates  in  the  bluffs  at  the  confluence  of  the 
Wisconsin  and  Mississippi  rivers;  its  total  length  is  about  85  miles. 
Two  points  are  noticeable;  one  is,  its  general  uniform  directness  of 
outline  (it  being  subject  to  but  few  and  unimportant  flexures);  and 
the  other  is  its  parallelism  with  the  Wisconsin  river,  so  long  as  the 
latter  holds  an  approximately  westerly  course;  the  summit  of  the 
ridge  being  always  about  fifteen  miles  from  the  river. 

The  divide  maintains  an  average  elevation  of  about  six  hundred 
feet  above  Lake  Michigan,  and  is  seldom  less  than  five,  or  more  than 
seven  hundred,  except  at  the  Blue  Mounds,  where  it  gradually  rises  east 


PLATE,  XXVII 


O  UTLI  N  E   M  A  P 
»////<» 

LE  AD    R  E  (V  I  O  N 

f.',i-/t//>/'fit/f/  f/ir  /Jnti>m.t/t>  ft/iff  t/ic 
/)/.<// •/' />n tit'ii  ftf  J*rn trie  an  ef  for -e,it . 


Tm:  M.i.wAru.r.  l.ini..  ,vf.» 


TOPOGRAPHY.  653 

and  west,  for  several  miles,  until  it  attains  an  elevation  at  the  west 
mound  of  1,151  feet.  This,  however,  is  an  extreme  case,  and,  in  fact,  the 
only  marked  exception  to  its  general  level.  In  the  town  of  Mount 
Hope,  a  slight  decrease  of  elevation  commences,  and  continues  to  the 
western  end  of  the  divide,  where  the  elevation  is  about  430  feet,  at  a 
point  within  a  mile  of  both  the  Mississippi  and  Wisconsin  rivers. 
There  are,  also,  two  main  branches  or  subdivisions  of  the  watershed; 
of  these,  the  western  is  the  ridge  which  separates  the  waters  that  flow 
into  the  Platfce  and  Fever  rivers,  from  those  which  flow  into  the  Peca- 
tonica.  It  leaves  the  main  divide  in  the  town  of  Wingville,  and  pas- 
sing through  the  townships  of  Belmont  and  Shullsburg,  in  a  south- 
easterly direction,  passes  out  of  the  state  in  the  town  of  Montieello. 
This  ridge  is  not  so  conspicuous  as  the  main  watershed,  eithei  for 
the  directness  of  its  course,  or  the  uniformity  of  its  elevation.  The 
most  conspicuous  points  on  it  are  the  Platte  Mounds,  which  appear 
from  a  distance  to  be  very  high,  but  are  in  reality  only  relatively  so, 
their  actual  elevation  being  only  about  seven  hundred  feet  above 
Lake  Michigan.  The  ridge  appears  to  slope  somewhat,  in  its  ap- 
proach to  Illinois,  its  average  elevation  there  being  about  500  feet. 

The  easterly  subdivision  is  that  which  separates  the  waters  of  the 
Pecatonica  and  Sugar  rivers.  It  may  be  said  to  begin  at  the  Blue 
Mounds,  or  a  couple,  of  miles  east  of  them,  and  pursuing  quite  a  de- 
vious course  through  the  .townships  of  Primrose,  Washington  and 
Monroe,  it  crosses  the  state  line  in  the  town  of  Jefferson.  This  ridge 
is  characterized  by  a  much  greater  want  of  uniformity  in  its  general 
course,  and  by  its  very  irregular  elevation.  It  is  much  narrower  than 
either  of  the  others,  more  abrupt  in  its  slopes,  and  contains  quite  a 
large  number  of  hills  and  low  places,  especially  in  the  towns  of  Prim- 
rose, Perry,  York,  and  New  (llarus,  in  which  towns  the  streams  head 
within  comparatively  short  distances  of  each  other,  on  opposite  sides 
of  the  watershed. 

These  are  the  principal  elevations  of  the  country  affecting  the  drain- 
age; there  are,  of  course,  many  minor  ones,  such  as  the  divides  be- 
t\veen  the  Grant  and  Platte  rivers,  or  the  several  branches  of  the  Pec- 
atonica; they  are,  however,  merely  subordinate  ridges,  and  are  but 
the  details  of  the  general  plan. 

Streams.  Having  thus  given  a  general  outline  view  of  the  sys- 
tem of  watersheds,  a  few  remarks  on  the  rivers  and  drainage  of  the 
Lead  region  are  necessary  to  supplement  them.  As  a  preliminary 
remark,  it  is  well  to  bear  in  mind,  that  their  present  situation  was 
probably  never  modified  or  influenced  by  drift  or  glacial  agencies;  the 
evidence  being  insufficient  to  prove  that  there  ever  was  any  drift  de- 


654:  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

posited  in  the  Lead  region,  the  probabilities  being  rather  to  the  con- 
trary. Premising  this,  it  follows,  that  the  location  of  streams  must 
have  depended  on  the  natural  configuration  of  the  country,  and  the 
superior  advantages  of  certain  strata  in  certain  positions,  predisposing 
them  to  become  the  beds  of  streams.  Other  things  being  equal,  sur- 
face waters  would  naturally  form  a  channel  first  in  the  more  soft  and 
easily  erosible  strata  lying  along  the  line  of  strike  of  some  soft  for- 
mation, and  would  cause  a  river  to  conform  its  first  channel  to  its  out- 
cropping edge.1  Simultaneously  its  tributaries  would  shape  their 
channels,  approximately  at  right  angles  to  the  river,  under  the  follow- 
ing conditions:  when  the  general  slope  and  drainage  of  the  country 
is  not  contrary  to  the  geological  dip  of  the  formations;  which,  in  the 
Lead  region,  does  not  appear  ever  to  have  been  the  case.  The  trib- 
utaries on  one  side  of  the  river  thus  formed  would  conform  them- 
selves to  the  natural  dip  of  the  underlying  strata,  sloping  toward  the 
main  river,  and  would  be  found  wherever  there  were  depressions,  or 
irregularities  in  the  surface,  suitable  to  their  formation.  These  would 
at  their  inception  approximate  to  their  final  length  and  course,  and 
future  changes  in  them  would  be  confiaed  to  the 'deeper  erosion  of 
their  beds,  and  widening  of  their  valleys;  the  formation  of  lateral 
branches;  the  division  of  the  head  of  the  stream  into  several  smaller 
sources,  and  finally,  the  gradual  recession  of  all  the  subordinate  parts. 

With  the  tributaries  on  the  other  side  of  the  principal  river,  a  dif- 
ferent order  would  prevail,  as  regards  their  position  and  growth. 
They  would  at  first  be  the  merest  rivulets,  and  increase  only  from  ero- 
sion ;  and  their  beds  would  lie  across  the  edges  of  the  strata.  There 
would  be  only  a  very  limited  extent  of  country  tributary  to  the  river 
on  this  side;  the  great  volume  of  its  water  being  derived  from  the 
tributaries  of  the  other  side.  The  dividing  ridge  would  thus  be  very 
near  the  river,  and  a  second  set  of  long  streams,  tributary  to  some 
other  river,  would  here  take  their  rise  and  flow  away. 

In  the  process  of  time,  the  main  river  would  slowly  cut  its  way 
through  the  soft  formation,  in  which  it  had  its  original  bed,  into 
and  through  those  which  underlaid  it.  This  might  at  first  be  accom- 
panied by  a  slight  recession  parallel  to  the  line  of  strike;  such  a 
movement,  however,  could  not  be  of  long  duration,  but  would  become 
less  as  the  valley  became  deeper;  because  any  such  recession  would 
necessitate  the  removal  of  all  the  overlying  formations.  Finally  the 
small  streams  flowing  across  the  strata  would  cut  their  valley  back 
from  the  river;  the  dividing  ridge  would  recede,  and  their  sources 
would,  from  the  position  of  the  strata,  be  in  steep  and  precipitous  ra- 
1  See  Report  of  Board  o£  Rearents  of  the  University  of  Minnesota,  for  1879,  pp.  46  and  47. 


TOPOGRAPHY.  655 

vines.  Such,  in  brief,  appears  to  be  the  theory  of  the  formation  of 
streams  in  the  Lead  region.  Its  application  is  easy,  and  would  be  as 
follows : 

The  Wisconsin  river  from.  Mazomanie,  to  its  mouth  near  Prairie 
du  Chien,  is  the  most  conspicuous  example  and  illustration  of  the 
foregoing  remarks. 

Although  the  surface  of  the  country,  in  its  present  condition,  does 
not  permit  the  accurate  delineation  of  the  former  lines  of  outcrop,  of 
the  paleozoic  formations;  yet  a  sufficient  number  of  outliers  remain, 
to  show  us  that  they  must  once  have  covered  the  country,  far  north 
of  where  they  are  at  present  found.  The  existence  of  Niagara  lime- 
stone, in  a  thickness  of  about  one  hundred  and  forty  feet  at  the  Platte 
Mounds,  and  probably  the  full  thickness  of  the  formation  at  the  Blue 
Mounds,  warrants  us  in  supposing  that  the  former  outcrop  of  the  un- 
derlying Cincinnati  group  was  at  least  as  far  north  as  the  present  bed 
of  the  Wisconsin  river. 

The  valley  now  occupied  by  the  river,  from  Mazomanie  to  Blue 
river,  is  very  nearly  that  of  the  present  line  of  strike  of  .the  Lower 
Silurian  formation,  and,  although  from  there  the  strike  of  the  lower 
members  (of  which  outliers  still  remain)  appears  to  bear  rather  more 
to  the  northward,  yet,  observations  on  the  dip  of  the  Cincinnati  group, 
in  such  occasional  outliers  as  remain,  lead  me  to  believe  that  its  origi- 
nal strike  was  approximately  in  a  southwesterly  direction,  from  Blue 
river  to  the  Mississippi. 

Assuming,  then,  that  the  Cincinnati  group  once  had  its  northern 
outcrop  where  the  river  now  runs,  or  in  a  line  parallel  to  it,  in  that 
vicinity,  the  surface  waters  would  easily  erode  a  channel  in  the  soft 
and  friable  shales  which,  to  a  great  extent,  compose  this  formation. 

In  fine,  the  whole  process  of  formation  previously  described  would 
take  place.  On  the  north  side  it  had,  as  now,  its  principal  tributary 
streams,  the  Kickapoo,  Knapp  creek,  Eagle  river,  Pine  river  and  Bear 
creek,  in  their  present  localities,  and  approximately  their  present 
length.  On  the  south  of  the  river,  however,  the  principal  watershed, 
already  referred  to,  was  probably  quite  near  the  river,  from  which 
position  it  has  receded  to  the  place  it  now  occupies.  The  Green  river, 
Blue  river,  Otter,  Mill  and  Blue  Mound  creeks  were  small  and  insig- 
nificant streams;  which,  by  the  gradual  process  of  erosion,  have  in- 
creased to  their  present  size  and  length;  but  even  now,  are  small  when 
compared  to  the  northern  tributaries. 

A  further  effect  was  to  shorten  the  Grant,  Platte,  and  Pecatonica 
rivers,  by  the  gradual  southwesterly  recession  of  the  watershed,  and 
the  lowering  of  the  latter  by  the  denudation  of  the  Niagara  limestone 


656  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

and  Cincinnati  groups;  except  in  such  localities  as  were  protected  bv 
a  superior  hardness  of  some  part  of  the  formation,  as  in  the  case  of 
the  Blue  Mounds. 

The  result  of  the  denudation  has  been  to  divide  the  country  into 
two  parts,  each  differing  widely  from  the  other  in  its  topographical 
features.  The  streams  flowing  southward  from  the  watershed  have 
eroded  the  country  into  gently  undulating  slopes.  This  is  probably 
due  to  the  direction  of  the  streams  conforming  in  a  measure  to  the 
dip  of  the  strata.  Abrupt  cliffs  and  steep  ravines  are  the  exception, 
and  not  the  rule,  never  being  found  in  the  immediate  neighborhood 
of  the  watershed,  but  rather  confined  to  the  small  lateral  branches. 
On  the  other  hand,  to  the  north  of  the  watershed,  the  panorama  of 
bluffs  and  precipitous  ravines  is  almost  mountainous  in  its  aspect. 
In  fact,  nothing  can  be  more  striking  than  the  contrast  which  pre- 
sents itself,  from  certain  points  on  the  divide,  in  looking  from  north 
to  south.  In  nearly  all  of  the  ravines  leading  northward,  the  fall  of 
the  first  quarter  of  a  mile  is  not  less  than  one  hundred  feet;  and,  in 
general,  it  is  true  of  the  streams  flowing  northward,  that  three- 
quarters  of  the  fall  takes  place  in  the  first  quarter  of  the  distance 
from  their  sources  to  their  mouth. 

It  seems  not  improbable  that  these  sudden  declivities  are  due  to  the 
streams  flowing  over  the  edges  of  the  strata,  rather  than  lengthwise 
along  their  dip.  Again,  the  streams  flowing  to  the  southward  become 
comparatively  sluggish  in  their  course,  as  soon  as  they  cease  to  be 
brooks.  They  have  usually  a  soft  muddy  bottom,  while  those  tributary 
to  the  Wisconsin  are  clear  and  rapid  streams,  flowing  over  a  sandy 
or  gravelly  bottom,  their  valleys  being  narrow  and  their  sides  very 
steep. 

The  streams  tributary  to  the  Platte,  Grant  and  Pecatonica  rivers  do 
not  exhibit  any  marked  characteristics  on  one  side  that  are  not  shared 
equally  by  the  other.  It  may  be  remarked,  however,  that  the  short 
streams,  which  flow  into  the  Mississippi  river,  present  much  the  same 
topographical  characteristics  as  are  seen  in  the  southern  tributaries 
of  the  Wisconsin,  narrow  and  deep  ravines  and  valleys,  being  ap- 
parently the  rule  in  the  western  part  of  Grant  county. 

The  Platte  river  is  frequently  found  inclosed  by  hills  which  are 
gently  sloping  on  one  side,  and  quite  precipitous  on  the  other.  This 
is  especially  noticeable  near  its  mouth.  The  river  in  such  cases  seems 
to  have  encroached  on  one  side  of  the  valley  for  a  long  period  of 
time,  producing  a  cliff  exposure  of  Lower  Magnesian  near  the  river, 
and  a  steep  bank  of  St.  Peters,  capped  with  a  more  retreating  slope  of 
the  Trenton,  as  shown  in  the  following  section.  [See  Fig.  1.] 


TOPOGRAPHY.  657 

In  this  connection  may  be  noticed  the  diminution  of  water  in  the 
Lead  region  since  the  early  mining  times.  In  comparing  the  streams 
at  present  with  those  recorded  in  the  government  surveys,  it  will  be 
fornd  that  many  of  the  smaller  ones  are  entirely  dry,  and  others 
nearly  so.  Numerous  springs,  which  formerly  furnished  an  abund- 
ant supply  of  water,  are  now  dry,  and  have  been  replaced  by  wells, 
sunk  to  obtain  water  from  a  deeper  stratum. 

FIG.  1. 


GENERAL  SECTION  OF  PLATTE  RIVER  VALLEY. 
1.  Trenton  Limestone.    2.  St.  Peters  Sandstone.    3.  Lower  Magnesian -Limestone. 

In  T.  5,  R.  6  W.,  are  several  streams  flowing  into  the  Mississippi 
river,  which  present  some  curious  features  in  common.  They  vary  in 
length  from  three  to  five  miles,  and  take  their  rise  in  the  Trenton 
limestone.  They  occupy  quite  long  and  narrow  valleys  of  erosion, 
and  their  dry  beds  may  be  distinctly  traced  in  them.  They  are  quite 
large  streams,  and  continue  increasing  in  size  for  a  mile  or  two  from 
their  sources,  until  they  reach  certain  beds  of  the  Lower  Magnesian 
formation,  when  they  gradually  disappear. 

The  large  streams  of  the  Lead  region  contain  a  much  smaller 
amount  of  water  than  heretofore.  Several  places  were  seen  where 
old  mills,  formerly  operated  by  water-power,  had  been  abandoned,  on 
account  of  a  diminishing  and  final  failure  of  the  supply. 

The  diminution  is  not  confined  to  surface  water,  springs,  streams 
and  the  like,  but  is  true,  to  a  greater  or  less  extent,  of  all  the  mining 
ground  of  the  region.  In  many  instances  this  circumstance  alone  has 
led  to  the  reopening  and  profitable  working  of  mines  which  years 
ago  were  abandoned  on  account  of  water,  with  ore  "going  down"  in 
the  crevices. 

It  is  probable  that  cultivation  of  the  land  is  the  chief  cause  of  this 
decrease,  as  a  much  greater  amount  of  surface  is  thus  exposed,  and 
evaporation  takes  place  more  rapidly  and  in  larger  quantities.  Re- 
moval of  the  timber  is,  without  doubt,  another  cause  of  this  decrease. 
The  soil  of  the  timbered  land  contains  more  moisture  than  that  of  the 
prairie;  and  in  all  countries,  the  removal  of  the  timber  has  always 
been  followed  by  a  marked  decrease  of  the  water  supply.  This  was 
Wis.  SUR.  —  42 


658  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

notably  the  case  in  the  Hartz  mountains,  of  Prussia,  after  the  fir  and 
hemlock  forests  were  removed.  When  the  mountain  sides  were  again 
planted  with  the  indigenous  trees,  by  order  of  the  government,  their 
growth  was  found  to  be  attended  by  an  increase  of  water  in  the 
streams  arid  springs. 

Springs  and  Wells.  The  Lead  region  is  one  of  the  best  watered 
tracts  of  country  in  the  state.  Springs  are  very  numerous,  both  about 
the  sources  of  the  streams  and  frequently  in  their  banks.  They  aro 
found  in  all  the  geological  formations,  but  with  the  greatest  frequency, 
and  of  the  largest  size,  between  the  bottom  of  the  Galena  limestone 
and  the  top  of  the  St.  Peters  sandstone.  Such  springs  are  usually 
found  flowing  along  the  surface  of  some  layer  of  clay,  and  finding  a 
vent  in  the  outcrop  of  an  opening.  The  clay  "openings  "  most  favor- 
able to  their  formation  are,  the  "  Upper  Pipe  Clay  opening,"  situated 
on  the  top  of  the  Blue  or  Trenton  limestone,  and  separating  it  from 
the  Galena  limestone;  the  "Glass  Hock  opening,"  separating  the 
Blue  and  underlying  Buff  limestone;  and  the  "Lower  Pipe  Clay 
opening,"  situated  in  the  lower  part  of  the  Buff  limestone;  the  latter 
however,  does  not  seem  to  be  so  persistent  a  bed  as  the  other  two. 
Springs  are  by  no  means  confined  to  these  three  openings,  but  occur 
in  many  of  the  beds  of  the  Galena  limestone,  as  well  as  in  the  lower 
formations;  usually,  however,  flowing  over  an  impervious  bed  of  clay, 
or  some  layer  of  rock  too  compact  to  admit  of  the  passage  of  water 
through  it. 

In  this  connection  it  is  desired  to  call  attention  to  the  springs  sit- 
uated about  150  feet  below  the  summit  of  the  west  Blue  Mound. 
They  have  been  attributed  by  many  persons  to  thermal,  igneous,  and 
other  deep-seated  agencies,  and  by  some  to  hydrostatic  pressure.  The 
following  facts  are  offered  in  regard  to  these  springs:  (1)  They  are 
found  at  intervals  on  all  sides  of  the  mound,  at  a  uniform  elevation, 
either  as  springs  or  low  wet  ground,  and  always  on  the  surface  of  a 
stratum  of  clay  impervious  to  water.  (2)  They  flow  most  abundantly 
during  and  after  rainy  seasons,  and  in  summer  are  frequently  nearly 
dry.  (3)  They  are  surmounted  by  the  cap  of  the  mound,  which  is  al- 
most a  solid  mass  of  flint,  and  presents  a  surface  of  about  100  acres 
as  a  watershed.  The  annual  rainfall  in  the  Lead  region  is  about  30 
inches,  of  which  about  one-quarter  is  removed  by  evaporation  and  the 
requirements  of  vegetation,  while  the  remainder  finds  its  way  to  the 
springs  and  streams.  On  the  one  hundred  acres  lying  above  the 
springs,  there  fall  annually  10,890,000  cubic  feet  of  water,  of  which 
three-quarters,  or  8,167,500  cubic  feet  pass  out  through  these  springs, 
which  seems  amply  sufficient  to  supply  them.  (4)  The  temperature 


TOPOGRAPHY. 


659 


of  the  Blue  Mound  springs  is  the  same  as  that  of  all  other  springs  in 
the  Lead  region,  which  is  about  the  mean  temperature  of  the  earth 
through  which  they  flow.  Were  they  thermal  springs,  or  of  igneous 
origin,  we  should  expect  to  find  at  least  some  lingering  traces  of  heat, 
to  show  us  from  whence  they  came.  In  view  of  these  facts,  it  seems 
more  logical  to  look  for  their  origin  in  the  natural  and  self  evident 
causes  presented,  than  to  attribute  them  to  more  complex  conditions, 
imperfectly  understood.  v 

FIG.  2. 


SKETCH  OF  THE  UPPEU  PART  OF  THE  BLUE  MOUNDS. 

1,  Flinty  cap  of  the  West  Mound;  2,  Horizon  of  the  springs;  3,  Niagara  limestone;  4,  Cincinnati 

group;  5,  Galena  limestone. 

In  such  portions  of  the  country  as  are  not  liberally  supplied  by 
nature  with  springs,  water  is  easily  and  abundantly  obtained  by 
means  of  wells.  Their  average  depth  is  about  twenty-five  feet;  this, 
however,  depends  chiefly  on  the  locality  in  which  they  are  sunk,  those 
on  the  ridges  and  prairies  being  deeper  than  the  rest.  Round  wells, 
of  four  or  five  feet  diameter,  are  usually  sunk  for  shallow  depths, 
sometimes  being  as  deep  as  sixty  feet.  Wells  are  sometimes  obtained 
by  drilling;  such  borings  being  chiefly  confined  to  the  prairie,  and 
seldom  exceeding  sixty  feet  in  depth.  They  are  then  furnished  with 
a  windmill  pump,  and  supply  an  abundance  of  clear  water  for  stock 
and  farm  purposes. 

Nearly  all  the  water  in  the  Lead  region,  whether  in  springs  or 
wells,  holds  in  solution  a  small  portion  of  lime  and  magnesia,  and 
a  still  smaller  quantity  of  sodium,  iron,  alumina,  and  silica.  The 
presence  of  these  salts  usually  gives  the  water  what  is  called  a  hard 
taste  which  is  more  noticeable  in  the  limestone  than  in  the  sandstone 
springs,  and  not  infrequently  induces  persons  to  believe  them  pos- 
sessed of  medical  properties. 

The  following  analysis,  which  is  believed  to  be  a  fair  sample  of  the 
quality  of  the  water  in  the  springs  and  wells  of  the  Lead  region,  is  in- 
serted to  show  the  small  amount  of  foreign  substances  which  they  con- 
tain. The  well  is  situated  on  the  K  E.  qr.  of  Sec.  9,  T.  2,  R.  9  E.,  a  short 
distance  northwest  of  the  city  of  Brodhead,  on  the  farm  of  Mr.  Freder- 
ick Gomber.  It  was  sunk  to  a  depth  of  about  thirty  feet,  of  which 


660  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

the  lower  part  (probably  about  ten  feet)  was  sunk  in  the  Lower  Mag- 
nesian  limestone,  the  rest  being  in  the  St.  Peters  sandstone. 

The  following  analysis  of  the  water,  by  Dr.  Gustavus  Bode,  of  Mil- 
waukee, was  furnished  by  Mr.  Goraber: 

One  gallon  II.  S.  standard  measure  contains  of  solid  salts,  13.2720 
grains,  consisting  of: 

Chloride  of  sodium 0.3248  grains. 

Sulphate  of  soda 0. 1792 

Bicarbonate  of  soda 0.0280 

Bicarbonate  of  lime * 6.6584 

Bicarbonate  of  magnesia 4.8552 

Bicarbonate  of  iron 0.2296 

Alumina •• - 0 . 1 288 

Silica 0.6888 

Organic  matter 0. 1792 

Total 13.2720   grs. 


Dr.  Bode  remarks  of  this  well  as  follows:  "The  total  amount  of 
salts  is  small  in  comparison  with  other  waters.  The  salts  themselves 
are  the  same  as  those  in  the  Waukesha  water,  and  in  the  same  com- 
bination. If  the  operation  of  this  water  depends  on  the  absence  of 
sulphuric  acid,  and  its  containing  bicarbonates,  so  the  same  good  and 
healing  results  may  be  expected  from  your  spring." 

Prairie  and  Forest.  The  prairie  area  of  the  Lead  region  is  com- 
paratively small,  and  seems  to  be  chiefly  a  continuation  of  the  great 
prairies  of  Illinois.  The  most  extensive  prairie  is  that  found  in  the 
southern  part  of  Grant  and  La  Fayette  counties,  comprising  the  town- 
ships of  Jamestown,  Hazel  Green,  Benton,  New  Diggings,  Shulls- 
burg,  Seymour,  Monticello  and  Gratiot.  From  this  there  is  a  branch 
extending  in  a  northwestern  direction  (corresponding  to  the  eastern 
subdivision  of  the  watershed  previously  alluded  to),  until  it  unites 
with  the  main  watershed;  here  it  branches  to  the  east  and  west.  The 
western  extension  forms  a  prairie  in  the  towns  of  Glen  Haven,  Patch 
Grove,  Little  Grant,  and  some  parts  of  Fennimore  and  "Wingville. 
The  eastern  prairie  follows  the  main  divide  already  described,  the 
prairie  being  from  six  to  ten  miles  in  width. 

Between  the  east  and  west  branches  of  the  Pecatonica,  there  is  a 
prairie,  including  most  of  the  towns  of  Fayette,  "Waldwick  and  Wiota. 
In  Green  county  the  principal  prairie  is  found  in  the  towns  of  Mon- 
roe, Clarno,  Sylvester  and  "Washington. 

This,  in  substance,  is  the  prairie  land  of  the  Lead  region,  although 
there  exist  small  isolated  patches  of  timber,  in  the  area  already  de- 
scribed, as  well  as  small  prairies,  or  openings,  in  the  remainder  of  the 


TOPOGRAPHY.  661 

region,  not  included  in  the  prairie  area,  and  which  is  mostly  timbered 
land.  The  original  area  of  prairie  appears,  from  the  government 
surveys,  to  have  been  somewhat  greater.  At  the  present  time,  the 
original  forests  of  large  timber  have  been  mostly  cut  down,  except 
about  the  Wisconsin  river  bluffs,  such  timber  as  is  now  found,  being 
a  second  growth,  of  black,  white  and  burr,  oaks,  maple,  hickory,  poplar 
and  elm,  the  trees  being  of  small  size,  seldom  more  than  a  foot  in  di- 
ameter. 

Mounds.  The  nearest  approach  to  mountains  in  the  Lead  region 
are  the  Platte  Mounds  in  La  Fayette  county;  the  Blue  Mounds  in 
Dane  and  Iowa  counties,  and  the  Sinsinawa  Mound  in  Grant  coun- 
ty. The  former  are  three  in  number,  about  a  mile  apart,  the  mid- 
dle one  being  very  small  in  comparison  with  the  other  two.  The 
east  and  west  mounds  are  about  the  same  elevation,  and  are  capped 
with  a  very  hard  Niagara  limestone  to  which  they  doubtless  owe 
their  preservation,  in  the  general  denudation  of  the  surrounding 
country.  The  ground  slopes  away  from  them  so  gently,  and  blends 
so  gradually  with  the  surrounding  high  land,  that  it  is  impossible  to 
define  exactly  where  the  mound  proper  begins. 

FIG.  3. 


~—Ztttie  Mount  ~~  fastJtfound 

SKETCH  OF  THE  PLATTE  MOUNDS. 
1  Niagara  limestone;  2  Cincinnati  group. 

The  Blue  Mounds  are  two  in  number;  one  being  in  Iowa  county, 
and  the  other  in  Dane.  The  top  of  the  west  mound  (which  is  the 
higher  of  the  two)  consists  of  over  a  hundred  feet  of  very  hard  flinty 
rock,  somewhat  resembling  quartzite;  below  this  is  the  Niagara  lime- 
stone. This  cap  of  quartz  rock  seems  to  have  been  removed  from  the 
east  mound;  the  top  of  which  is  a  flat  table  land  under  cultivation. 
These  mounds  are  very  conspicuous,  and  can  be  seen  from  any  mod- 
erately high  land  in  the  Lead  region. 

The  Sinsinawa  Mound  is  also  a  very  conspicuous  object,  in  the 
southern  part  of  Grant  county,  near  the  village  of  Fairplay.  It  is 
composed,  for  the  most  part,  of  the  Cincinnati  group,  capped  with  a 
small  amount  of  Niagara  limestone. 

Sinks.  Very  remarkable  features  in  the  vicinity  of  the  Blue 
Mounds  are  the  numerous  sink  holes  found  near  their  base,  and  fre- 
quently quite  high  up  on  their  sides.  These  sinks  are  usually  in 
groups  of  three  or  four,  and  invariably  in  nearly  an  east  and  west 


662  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

line.  One  group  is  near  the  former  residence  of  Ebenezer  Brigham, 
at  the  foot  of  the  East  Blue  Mound,  in  the  S.  W.  qr.  of  Sec.  5,  T.  6, 
R.  6  E.  There  are  about  a  dozen  of  them,  nearly  round,  varying  in 
diameter  from  ten  to  twenty  feet,  and  about  five  feet  deep,  all  in  a 
line,  bearing  about  10°  north  of  west.  At  the  West  Blue  Mound 
there  are  several  lines  of  them,  about  the  base  and  side  of  the  rnound. 
On  the  center  line  of  Sec.  1,  T.  6,  R.  5  E.  there  is  a  well  defined  line 
of  them,  extending  for  about  a  quarter  of  a  mile  on  each  side  of  the 
center  of  the  section.  There  is  another  range  of  them  near  the 
center  of  the  S.  W.  qr.  of  Sec.  1,  and  a  third  line  near  the  quarter 
post  of  Sees.  1  and  12.  The  largest  of  these  sinks  is  an  isolated  one 
near  the  center  of  the  S.  E.  qr.  of  Sec.  1,  which  is  as  much  as  fifty 
feet  in  diameter,  and  twenty  feet  deep.  In  this  one  the  wall  rock  of 
the  fissure  could  be  very  plainly  seen  on  the  south  side.  From  tho 
circumstance  of  their  direction  and  position  coinciding  with  that  of 
all  the  mineral  crevices  in  the  vicinity,  and  the  fact  that  the  ore  is 
always  found  in  large  crevice  openings,  the  inference  seems  to  be  that 
these  sinks  mark  the  line  of  large  open  crevices  in  the  rock  beneath 
them.  It  is  also  reasonable  to  suppose  that  the  sinks  along  the  cen- 
ter line  of  Sec.  1,  T.  6,  R.  5  E.  are  a  continuation  of  those  near  the 
Brigham  place,  as  they  seem  to  point  almost  directly  to  one  another. 
It  is  probable  that  the  water,  percolating  through  the  earth  into  these 
crevices,  has  in  process  of  time  carried  so  much  of  the  soil  with  it 
as  to  cause  a  falling  in  of  the  surface,  leaving  the  sinks  as  the  result. 
In  view  of  the  vast  quantity  of  ore  which  has  in  former  times  been 
obtained  from  the  crevice  openings  in  this  locality,  it  would  seem  to 
be  worth  while  to  prospect  some  of  these  sinks;  but  nothing  of  the 
kind  has  ever  been  done. 

Sinks  do  not  appear  to  be  confined  to  the  Galena  limestone,  but 
seem  to  be  quite  as  frequent  at  the  Blue  Mounds  in  the  Niagara 
formation.  They  have  been  observed  in  many  other  localities  in  tho 
Lead  region.  The  following  are  cited,  to  show  their  occurrence  in 
the  several  formations.  On  the  S.  E.  qr.  of  Sec.  14,  T.  5,  R.  2  W., 
are  three,  situated  in  a  triangular  form,  in  the  St.  Peters  sandstone. 
This  is  somewhat  exceptional,  as  the  sink  holes  are  usually  confined 
to  the  limestone  formations.  On  the  S.  hf.  of  Sec.  11,  T.  6,  R.  4  E., 
are  several  of  these  sink  holes,  from  eight  to  twelve  feet  deep. 

The  largest  one  noticed  is  situated  on  the  summit  of  the  ridge,  on 
the  S.  E.  qr.  of  Sec.  29,  T.  6,  R.  2  E.  It  lies  in  the  Galena  limestone, 
and  is  about  200  feet  long,  by  100  wide,  and  about  twenty  feet  deep. 


SURFACE  GEOLOGY.  663 

SURFACE  GEOLOGY. 

Soil  and  Subsoil.  The  quality  of  the  soil  of  the  Lead  region  is 
chiefly  dependent  on  the  character  of  the  subjacent  formations.  The 
subsoil  appears  to  be  derived  directly  from  the  decay  and  disintegra- 
tion of  the  strata,  of  which  it  is  the  residuum.  South  of  the  princi- 
pal watershed,  the  subsoil  is  clay,  almost  without  exception,  having 
a  thickness  of  from  three  to  six  feet,  depending  on  the  configuration 
of  the  underlying  rock  formation.  This  is  the  average  thickness,  on 
comparatively  level  land;  on  side  hills  it  is  usually  much  thinner,  the 
greater  part  having  been  washed  down  into  the  valley  below.  The 
clay  soils  and  subsoils  appear  to  consist  chiefly  of  those  portions  of 
the  overlying  Galena  limestone,  and  earthy  Cincinnati  shales,  which 
being  insoluble  in  water,  were  not  removed  by  the  gradual  process  of 
denunation. 

The  amount  of  lime,  magnesia,  and  alkaline  earths  in  the  subsoil 
and  soil,  together  with  the  vegetable  mold  in  the  latter,  constitute  a 
soil,  which,  in  its  virgin  state,  is  unsurpassed  for  richness  and  fertil- 
ity. The  number  of  successive  wheat  crops  which  have  been  raised, 
without  regard  to  rotation,  on  some  of  our  prairie  farms,  attest  its 
native  strength;  as  also  the  marked  decline  in  fertility  of  the  soil 
when  this  has  been  done,  shows  the  inevitable  retribution  which  fol- 
lows the  practice. 

Exceptions  to  the  clay  soil,  usually  found  in  the  country  covered 
by  the  Galena  limestone,  are  found  in  the  eastern  part  of  La  Fayette, 
and  frequently  in  Green  county,  where  the  soil  is  quite  sandy,  owing 
to  the  disintegration  of  calcareous  sand  layers  frequently  found  there 
in  that  formation.  A  few  localities  are  cited  below,  where  the  sand 
was  so  abundant,  that  the  formation  might  have  been  considered  a 
sandstone,  were  it  not  for  the  occasional  outcrops  of  Galena  limestone 
in  place.  In  the  western  part  of  the  town  of  Jordan,  T.  2,  E.  6  E., 
in  sees.  2,  11  and  14,  the  ridges  have  a  great  deal  of  sand  contained 
in  the  soil.  The  roads  are  frequently  sandy,  similar  to  those  in  a 
sandstone  formation.  Lying  entirely  without  the  limits  of  the  Drift, 
this  circumstance  led  to  a  search  for  and  discovery  of  the  original 
beds. 

At  the  village  of  Martin,  in  the  S.  E.  qr.  of  sec.  32,  T.  1,  E.  6  E., 
on  the  Fecatonica  river,  at  the  saw-mill,  is  a  large  stone  quarry,  of 
which  the  upper  portion  consists  of  Galena  limestone  in  thin  beds, 
containing  considerable  calcareous  sand  between  the  layers.  This  is 
the  first  locality  where  the  sand  was  found  in  place. 

On  the  ridge  near  the  quarter-post  of  29  and  32,  T.  2,  E.  6  E.,  a 


664:    GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

great  deal  of  sand  was  seen  at  an  elevation  of  150  feet  above  the  top 
of  the  St.  Peters;  numerous  concretions  of  iron  were  also  found,  sim- 
ilar to  those  usually  found  in  the  upper  bed  of  that  formation.  East 
of  the  center  of  sec.  34,  T.  3,  R.  6  E.,  is  another  sandy  ridge. 

The  agencies  of  the  glacial  period  do  not  appear  to  have  had  any- 
thing to  do  with  transporting  the  component  materials  of  the  soil, 
and  although  a  slight  transportation  has  taken  place,  it  is  always 
merely  local.  For  instance,  in  the  valleys  of  the  creeks  which  lie  in 
the  St.  Peters  sandstone,  the  soil  is  usually  a  rich  clay  loam,  richer 
in  fact  than  that  of  the  adjacent  ridges,  because  the  best  parts  of  the 
upland  soils  have  been  washed  down,  and  distributed  over  the  surface 
of  the  valley. 

A  similar  transportation  may  be  observed  in  passing  up  any  long, 
and  moderately  steep  hill,  which  includes  several  formations;  such 
hills  being  very  common  north  of  the  principal  watershed.  Let  us 
suppose  one,  whose  summit  is  composed  of  Galena  limestone,  and 
whose  base  lies  in  the  Lower  Magnesian.  Scattered  about  the  base 
will  be  seen  many  loose  pieces  of  Lower  Magnesian  limestone,  mixed 
with  less  numerous  bowlders  of  St.  Peters  sandstone;  still  less  nu- 
merous and  smaller  pieces  of  the  Buff  and  Blue  (Trenton)  limestone, 
while  fragments  of  the  Galena  limestone  will  be  comparatively  rare. 
On  ascending  the  hill  and  arriving  at  the  St.  Peters,  fragments  of 
Lower  Magnesian  will  no  longer  be  seen ;  while  those  of  the  upper 
formation  will  become  larger  and  more  numerous.  On  arriving  at 
the  Buff  limestone,  the  fragments  of  St.  Peters  sandstone  will  also 
have  disappeared,  fragments  of  Blue  limestone  will  be  very  numerous 
and  easily  recognized  by  their  white  color,  and  their  general  rounded 
and  v/orn  appearance.  On  reaching  the  summit  of  the  hill,  no  frag- 
ments of  stone  will  be  found,  except  such  as  are  derived  from  the 
subjacent  Galena  limestone.  One  prominent  feature  of  the  soil  will 
be  the  prevalence  of  flints,  which  are  nearly  indestructible,  and  often 
form  a  large  component  part.  From  the  arrangement  of  the  surface 
soil  and  fragmentary  rock,  it  is  evident  that  the  rock  of  any  formation 
is  never  found  above  the  level  from  which  it  was  detached. 

Peat.  While  on  the  subject  of  surface  soil  and  subsoil,  it  is  de- 
sired to  'report  two  places  in  Green  county  which  afford  the  only  ap- 
proach to  this  useful  article,  which  has  been  observed  in  the  Lead 
region.  The  first  is  situated  on  Jordan  creek,  in  the  E.  hf.  of  Sees. 
21  and  28,  T.  2,  R.  6  E.,  and  comprises  f  roni  one  hundred  and  fifty  to 
two  hundred  acres.  The  other  locality  is  on  the  Little  Sugar  river, 
near  the  center  of  Sec.  11,  T.  3,  R  7  E.  As  the  conditions  under 
which  they  exist  are  similar,  one  description  will  serve  for  both. 


SURFACE  GEOLOGY.  665 

The  turf  is  underlaid  by  an  impervious  stratum  of  blue  clay,  which 
holds  the  water  and  nourishes  a  vegetable  growth  about  four  feet 
thick,  which,  in  this  section  of  the  country,  is  known  as  peat.  AV^hen 
cut  and  dried,  it  burns  similarly  to  peat,  but  with  so  large  a  residuum 
of  clay,  sand  and  ashes,  as  to  render  it  unfit  for  economic  purposes. 

Brick  Clay.  Clay  suitable  for  making  brick  is  found  in  many 
parts  of  the  Lead  region.  Among  the  localities  are  Lancaster,  Min- 
eral Point  and  Platteville.  The  first  has  two  yards  in  operation,  and 
the  latter  has  one,  which  commenced  operations  in  the  spring  of  1874. 
The  clay  used  is  usually  of  a  grayish-yellow  color  which  becomes  red 
on  burning.  It  appears  to  have  been  formed  in  the  same  manner  as 
other  portions  of  the  soil,  as  already  described. 

In  the  Platteville  yard  an  opportunity  was  found  to  see  the  process 
of  manufacture.  The  clay  is  dug  from  an  adjacent  bank,  some  selec- 
tion being  necessary.  It  is  then  run  on  small  cars  to  the  pug-mills 
(which  are  three  in  number)  and  ground  with  water,  until  it  forms  a 
homogeneous  paste.  After  this  comes  the  moulding  into  bricks, 
which  are  spread  out  on  the  floor  of  the  yard,  dried  and  piled  in  a 
kiln  to  burn.  A  kiln  of  these  bricks  takes  about  eight  days  to  burn. 
It  is  estimated  that  about  8,000  bricks  per  day  can  be  made  in  this 
yard. 

In  the  city  of  Monroe,  in  Green  county,  is  a  brick  yard  where  two 
kinds  of  brick  are  made  from  the  same  kind  of  clay.  One  is  a  red 
brick,  similar  to  all  common  red  brick;  the  other  is  a  cream-colored 
brick,  of  very  handsome  appearance,  closely  resembling  the  Milwaukee 
brick.  From  the  lalter,  many  of  the  handsomest  buildings  in  Monroe 
are  constructed.  The  difference  in  color  is  due  to  the  difference  in 
burning,  the  red  color  being  caused  by  a  greater  and  long  continued 
heat. 

The  origin  of  the  clay  of  which  the  brick  are  made  is  a  matter  of 
some  doubt.  It  does  not  have  exactly  the  appearance  of  a  drift  clay ; 
and  if  not,  its  situation  indicates  that  it  must  have  undergone  some 
subsequent  rearrangement. 

Glacial  Drift.  As  has  been  before  intimated,  the  Lead  region  is 
a  driftless  tract  of  country;  not  a  single  bowlder,  pebble  or  clay  of 
foreign  origin  being  found  in  its  limits,  except  in  three  or  four 
isolated  cases,  which  will  be  hereafter  described. 

The  northern  boundary  line  of  the  driftless  region  lies  far  to  the 
north  of  the  Lead  region.  The  eastern  line  was  found  in  Green 
county,  and  traced  out  with  all  possible  accuracy.  For  a  particular 
description  of  it,  reference  is  made  to  the  geological  maps;  in  brief, 
however,  it  is  as  follows:  It  commences  on  the  west  side  of  the  Pec- 


666  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

atonica  river,  crossing  the  state  line  at  the  southwest  corner  of  the 
town  of  Cadiz.  From  here  it  proceeds  almost  in  a  straight  line  to  the 
city  of  Monroe.  Thence  north,  it  runs  along  the  divide  between  the 
Pecatonica  and  Sugar  rivers,  until  about  two  miles  south  of  New 
Glarus,  where  it  takes  a  northeasterly  course,  and  passes  out  of  the 
county  about  a  mile  west  of  Belleville.  The  course  thus  indicated  is 
its  present  line  as  shown  by  erratic  bowlders  lying  upon  the  surface. 
If  the  drift  deposits  originally  extended  farther  westward,  no  trace 
thereof  now  remains.  East  of  the  line  described,  bowlders  are  found 
in  all  parts  of  the  county,  with  more  or  less  frequency.  The  boun- 
dary line,  where  bowlders  are  now  found,  does  not  appear  to  conform 
at  all  to  the  surface  features,  but  crosses  the  valleys  of  the  streams, 
and  the  ridges  between  them,  with  equal  impartiality. 

The  different  kinds  of  rock  found  in  the  drift  are  so  numerous  that 
it  would  require  quite  a  catalogue  to  enumerate  them  all.  It  will  be 
sufficient  to  state  that  the  great  bulk  of  them  are  granitic,  metamor- 
phic,  or  trappean;  the  most  frequent  being  varieties  of  granite  and 
gneiss,  and  next  to  them  the  trappean  rocks;  chloritic  rocks,  and  those 
of  a  schistoze  structure,  are  also  quite  numerous. 

In  addition  to  these  there  are,  in  certain  places,  beds  of  gravel,  sand 
and  clay.  The  distribution  of  the  bowlders  does  not  appear  to  be 
very  regular  in  Green  county,  in  fact,  the  whole  of  the  county  verges 
so  near  the  western  boundary  of  the  drift,  that  comparatively  small 
deposits  were  made  here,  which  are  quite  insufficient  to  exemplify  any 
general  laws  of  distribution.  No  difference  could  be  seen  in  their 
frequency,  between  the  eastern  line  of  the  county  and  the  western  line 
of  the  drift. 

The  bowlders  are  of  various  sizes,  from  a  few  inches  to  two  or  three 
feet  in  diameter,  and  are  always  rounded  and  worn  smooth.  They  are 
frequently  found  quite  numerous  in  one  place,  and  then  scattered 
along  at  very  distant  intervals,  on  the  same  kind  of  ground,  but  do 
not  exhibit  any  distinctive  morainic  appearance. 

Gravel  beds  are  not  very  frequent,  although  they  are  found  in  sev- 
eral places  in  Green  county.  There  is  one  situated  very  near  the 
boundary  of  the  drift,  on  the  1ST.  W.  qr.  of  Sec.  4,  T.  1,  R.  7  E.,  where 
there  is  a  bed  of  gravel  about  eight  feet  thick,  underlaid  by  a  bed  of 
stratified  sand  and  clay  about  four  feet  in  thickness.  This  sand  is 
very  fine,  and  has  just  enough  clay  mixed  with  it  to  make  a  good  ar- 
ticle of  moulding  sand  for  iron  foundries;  it  would  give  a  fine  impres- 
sion, and  make  a  smooth  casting.  A  similar  bed  was  found  about 
two  miles  east  of  the  preceding,  in  the  S.  W.  qr.  of  Sec.  2,  T.  1,  R. 
7  E.,  where  the  drift  sand  and  gravel  have  accumulated  to  a  thickness 


PLATEJHOX 


(iniittinj^ 


flag  ] 


SURFACE  GEOLOGY.  667 

of  about  twelve  feet.  A  large  amount  of  it  lias  been  utilized  for 
railroad  ballast.  A  third  bed,  like  the  other  two,  was  observed  on 
the  N.  E.  qr.  of  Sec.  2,  T.  1,  R.  7  E.,  also  several  others  in  various 
portions  of  the  county.  Those  already  described  will  serve  as  sam- 
ples of  all. 

The  amount  of  drift  clay  in  Green  county  is  comparatively  small, 
it  probably  having  been  dissolved  out  and  washed  away  from  the 
greater  portion  of  the  surface.  It  was  only  observed  in  one  pl.'tce,  in  the 
~N.  "W.  qr.  of  Sec.  25,  T.  3,  R.  7  E.,  where  a  well  had  been  sunk  in 
the  drift.  There  was  here  a  thickness  of  about  twenty  feet  of  slate- 
colored  clay,  full  of  small  pebbles. 

Outside  of  Green  county,  the  indications  of  drift  observed  were  so 
few  and  imcertain,  that  it  seems  scarcely  proper  to  attribute  them  to 
glacial  agencies,  and,  on  the  other  hand,  there  is  great  difficulty  in 
accounting  for  them  in  any  other  manner.  They  are  briefly  as  fol- 
lows: 

Prof.  Whitney  describes,  on  page  137  of  the  report  of  1862,  a  group 
of  loose  blocks  of  sandstone,  which  are  situated  as  he  represents  them 
in  his  wood  cut.  It  is  referred  to  in  this  connection,  because  I  de- 
sire to  report  with  it  two  similar  deposits,  which  have  been  observed. 
The  first  is  situated  on  the  road  from  Mineral  Point  to  Dodgeville, 
on  the  S.  E.  qr.  of  Sec.  9,  T.  5,  R.  3  E,  as  much  as  three  miles  from 
any  outcrop  of  the  St.  Peters  sandstone.  The  bowlders  are  from  one 
to  two  feet  in  diameter,  and  lie  scattered  along  the  road,  and  in  the 
adjacent  fields,  on  the  south  slope  of  the  hill.  The  bowlders  are  none 
of  them  very  large,  and  it  is  not  impossible  that  they  were  hauled 
there,  although  it  is  difficult  to  understand  for  what  purpose.  There 
are  not  now,  nor  have  there  ever  been  any  houses  near  them. 

The  second  locality  is  on  the  1ST.  E.  qr.  of  Sec.  5,  T.  1,  R.  2  E.,  on 
the  ridge  between  the  Strickland  and  Myers  branches.  There  are 
here  quite  a  number  of  blocks  of  St.  Peters  sandstone  lying  on  the 
summit  of  the  ridge.  The  blocks  are  of  various  sizes,  some  of  them 
weighing  several  tons.  These  bowlders  are  more  distant  from  any 
outcrop  of  sandstone  than  either  of  the  others;  the  nearest  being  at 
"  Cook's,"  about  five  miles  to  the  northwest,  in  Sec.  22,  T.  2,  R.  1  E. 
It  is  somewhat  singular  that  these  isolated  bowlders  should  always  bo 
of  sandstone.  These  several  instances  have  been  cited  as  quite  remark- 
able and  singular  exceptions  to  the  general  driftless  character  of  the 
Lead  region,  although  we  have  no  very  plausible  theory  to  account  for 
their  origin. 


668  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


CHAPTEE  III. 
GEOLOGICAL  FORMATIONS. 

POTSDAM  SANDSTONE. 

Geographical  Boundaries.  South  of  the  Wisconsin  river  it  is 
found  as  the  bed  rock  of  Otter,  Mill  and  Blue  Mounds  creeks,  and 
their  various  tributaries,  as  far  south  as  town  7,  on  the  various  ranges. 

7  7  £5 

Here  it  disappears,  owing  to  the  southerly  dip  of  the  formation,  and 
the  sudden  rise  of  the  country  to  the  south.  The  valley  of  the  Wis- 
consin river  also  lies  in  this  formation,  forming  a  very  level  plain 
from  two  to  three  miles  wide,  and  extending  from  Sauk  City  to  a 
point  about  four  miles  above  the  mouth  of  the  river.  Good  natural 
exposures  are  seen  in  the  bluffs  on  each  side  of  the  river,  in  which  the 
various  strata  may  be  traced  uninterruptedly  for  miles. 

The  greatest  exposed  thickness  is  seen  in  the  valley  of  the  Wiscon- 
sin river,  where  it  is  about  300  feet  from  the  water  to  the  bottom  of 
the  Lower  Magnesian  limestone.  Examinations  north  of  the  Wiscon- 
sin river  make  the  entire  thickness  of  the  formation  about  1,000  feet. 

Lithological  Characteristics.  The  following  section,  taken  from  a 
bluff  about  three  miles  northwest  of  Lone  Rock,  in  the  IS".  E.  qr.  of 
Sec.  34,  T.  9,  R.  2  E.,  will  serve  as  a  general  guide  to  the  formation : 

i  A.    Lower  Magnesian  Limestone. 

1.  Irregularly-bedded,  white  and  yellowish  Lower  Magnesian  limestone,  con-    ft-    /». 

taining  no  flints 60 

2.  Transition  beds  of  arenaceous  limestone,  in  which  rounded  grains  of  sand 

are  cemented  together  by  limestone 5 

B.     Potsdam  Sandstone. 

3.  Sandstone,  white,  very  heavy-bedded,  containing  at  the  bottom  occasional 

horizontal  seams  of  lime.    Friable 45 

4.  Thin-bedded,  earthy,  straw -yellow  shales,  containing  Dicellocephalus  and 

Lingula 45 

5.  Very  finely  laminated  blue  shale 3 

6.  Thin-bedded,  yellow,  argillaceous  limestone 2 

7.  Earthy  material 3 

8.  Very  hard  and  compact  brown  limestone,  building  stone 4 

9.  Thin-bedded  gray  limestone,  building  stone 9 

10.  Yellow  and  white  friable  sandstone,  to  the  valley,  mostly  unexposed,  cov- 
ered by  slope  of  hill •  •  •  190     . . 

Total  thickness 360      6 


PLATE.XXXT 


1  ljmn.lt  F.tttlK tr, 


GEOLOGICAL  FORMATIONS.  669 

The  beds  mentioned  under  Nos.  8  and  9  change  to  a  yellow,  arena- 
ceous limestone,  which  is  extensively  quarried  for  building  stone  at 
Mazomanie,  Black  Earth  and  other  towns  in  the  vicinity.  It  is  easily 
quarried  and  dressed,  and  makes  a  good  and  durable  building  stone, 
which  does  not  undergo  much  change  on  exposure  to  the  weather. 
The  sandstone  is  but  little  used  for  building  stone,  as  it  is  too  friable. 

The  sandstone  beds  of  the  Potsdam  are  usually  composed  of  a  very 
soft  and  friable  sand,  frequently  crumbling  readily  between  the  fin- 
gers, especially  if  it  is  white.  The  upper  beds  are  more  frequently 
white  than  the  others,  although  white  beds  are  not  uncommon  in  all 
parts  of  the  formation.  In  general,  the  lower  beds  are  yellow  or 
brownish  in  color.  The  great  inequality  in  the  hardness  of  the  sev- 
eral strata  of  the  Potsdam  is  frequently  the  cause  of  the  formation  of 
terraces  by  erosion,  which  are  often  a  conspicuous  feature  of  the 
valleys  in  the  vicinity  of  the  Wisconsin  river.  The  following  section 
of  a  hill  near  Lumberville,  on  the  Wisconsin,  illustrates  their  ap- 
pearance. 

FIG  4. 


SKETCH  OP  A  TERRACED  HILL  NEAR  LUMBEKVILLE. 

1.  Lower  Magnesian  Limestone.     2.  White  Potsdam  Sandstone.     3.  Fossiliferous  Shales. 
4  and  5.  Dolomitic  Beds.    6  and  7.  Dark-colored  Sandstone. 

South  of  the  Wisconsin  river,  about  the  head-waters  of  Blue 
Mounds  creek,  and  Mill  creek,  the  upper  bed  of  the  Potsdam  consists 
of  a  red  and  very  ferruginous  sandstone,  often  containing  seams  of 
iron  ore,  and  iron  concretions.  The  coloring  matter  appears  to  be 
partially  soluble,  and,  becoming  washed  out  by  the  rain,  colors  the 
soil  in  some  places  to  a  considerable  extent.  It  is  quite  conspicuous 
at  Mr.  Ruggles'  farm,  on  the  road  from  Dodgeville  to  Arena.  It 


670  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

was  found  in  a  tract  of  land  about  six  miles  long,  east  and  west,  and 
about  five  miles  wide,  north  and  south.  Another  locality  where  it  is 
very  conspicuous  is  near  the  center  of  Sec.  17,  T.  7,  R.  4  E.  In  a 
ditch  by  the  side  of  the  road,  it  appears  as  a  very  dark-red  sandstone, 
streaked  occasionally  with  yellow,  and  overlaid  by  a  dark-brown, 
earthy,  ferruginous  shale. 

Along  the  road  for  some  distance  above  this  outcrop,  there  is  a 
sandstone  containing  seams  of  iron  ore.  The  formation  appeared  to 
be  about  sixty  feet  thick  and  unfossiliferous.  The  country  here  is  so 
deeply  covered  with  fallen  rock,  from  the  overlying  formations,  that 
it  is  difficult  to  determine  the  precise  horizon  of  the  different  beds. 
The  same  beds  were  traced  out  to  the  K.  "W.  qr.  of  Sec.  7,  T.  7,  R.  4: 
E.,  where  they  present  the  same  appearances.  In  each  of  these  local- 
ities, the  thickness  of  the  overlying  Lower  Magnesian  does  not  exceed 
100  feet. 

From  the  results  of  certain  experiments  instituted  upon  the  shales 
designated  in  the  section  as  No.  4,  we  are  inclined  to  think  they 
would  make  a  tolerable  quality  of  hydraulic  lime,  although  they  are 
not  sufficiently  quick-setting  to  make  a  good  hydraulic  cement. 

It  will  be  seen  from  an  inspection  of  the  foregoing  section,  that  no 
sandstone  is  included  in  the  Lower  Magnesian  formation  which  ex- 
tends to  B.  Some  geologists,  however,  place  the  line  dividing  the 
two  formations  between  the  beds  numbered  nine  and  ten  under  B  in 
the  section,  p.  668,  thus  including  the  Dicellocephalus  shales  and  lime- 
stones, as  well  as  the  upper  bed  of  sandstone,  in  the  Lower  Magne- 
sian formation,  and  beginning  the  Potsdam  with  the  bed  numbered 
ten.  If  this  arrangement  were  adopted,  the  Lower  Magnesian  would 
sum  up  as  follows:  Limestone  above  the  sandstone  bed  No.  3  of  the 
section,  full  thickness,  250  feet;  sandstone,  45  feet;  shales  and  lime- 
stone, 61  feet,  making  a  total  of  356  feet,  which  is  much  greater  than 
has  heretofore  been  attributed  to  the  formation.  On  the  whole,  it  has 
seemed  best,  on  paleontological  grounds,  for  the  sake  of  "perspicuity, 
and  to  avoid  confusion  in  comparison  with  other  reports,  to  respect 
the  old  landmarks,  of  subdivision,  especially  as  bed  No.  4  contains 
the  characteristic  Potsdam  fossils. 

Paleontology.  The  fossil  remains  of  this  formation  seem  to  bo 
chiefly  confined  to  the  calcareous  strata  and  argillaceous  shales,  de- 
scribed under  numbers  4  and  6  of  the  foregoing  section,  the  most 
productive  being  those  which  immediately  overlie  the  limestone 
quarry  rock.  All  the  quarries  from  Black  Earth  to  Boscobel  were 
examined,  and,  in  all,  more  or  less  specimens  were  found.  The  re- 
mains consist  chiefly  of  JLingula  aurora  and  Dicellocephelus  Minne- 


GEOLOGICAL  FORMATIONS.  671 

sotensis,  the  former  being  quite  small,  and  usually  having  the  shell 
remaining;  sometimes,  however,  the  shells  have  been  ground  up  so 
that  only  a  few  fragments  are  found,  disseminated  through  the  shales. 
The  trilobites  are  seldom  or  never  found  entire,  but  usually  the 
cephalic  portion,  the  pygidium,  or  still  smaller  fragments.  The  vari- 
ous sandstone  beds  of  the  Potsdam  are  usually  unfossiliferous.  The 
upper  bed  of  sandstone  seldom  contains  anything  but  Scolithus,  which 
in  some  localities  is  very  numerous.  This  fossil  is  also  frequently 
found  in  all  the  sandstone  beds. 


LOWER  MAGNESIAN  LIMESTONE. 

Geographical  Boundaries.  South  of  the  Wisconsin  river  and 
north  of  the  main  watershed,  it  occupies  a  tract  of  land  lying  about 
the  heads  of  all  the  smaller  tributary  streams,  although  seldom  found 
so  far  back  as  their  springs.  Passing  down  any  of  the  streams,  such 
as  Otter  creek  or  Mill  creek,  we  gradually  pass  below  its  surface;  and 
its  outcrops  are  seen  gradually  higher  in  the  hills,  until,  on  reaching 
the  Wisconsin  river,  it  forms  the  cap  of  all  the  bluffs  from  Sauk 
City  to  Boscobel,  usually  appearing  in  bold  and  rugged  cliffs,  lend- 
ing a  very  picturesque  effect  to  the  scenery  of  the  river.  It  forms 
also  the  valley  of  the  Wisconsin  for  about  four  miles  above  its  mouth, 
and  the  valley  of  the  Mississippi  as  far  south  as  Glen  Haven,  where 
it  passes  beneath  the  surface.  Passing  south  of  the  divide  which 
separates  the  waters  which  flow  into  the  Wisconsin  from  the  Pecato- 
nica,  it  is  found  in  the  branches  of  the  latter  stream,  as  far  north  as 
the  north  line  of  to\vn  5  in  ranges  5  and  6  E.  Proceeding  westward, 
it  is  not  again  encountered  until  the  Platte  and  Grant  rivers  are 
reached,  where  it  is  found  as  the  bed-rock  of  those  streams,  and  in 
T  5,  R.  3  W.,  it  covers  a  large  portion  of  the  township. 

In  Green  county,  there  is  but  one  exposure  of  the  formation.  It 
is  in  the  valley  of  the  Sugar  river,  about  three  miles  above  Brodhead. 
It  commences  a  short  distance  north  of  the  center  of  Sec.  15,  T.  2,  R. 
9  E.,  where  it  has  a  width  of  about  half  a  mile.  In  passing  into  town 
three,  it  widens  to  nearly  two  miles.  It  then  becomes  narrower,  at- 
tains its  greatest  elevation  above  the  river  at  Albany,  and  finally  dis- 
appears beneath  the  surface  of  the  river  about  a  mile  and  a  half  above 
that  village. 

Lithological  Characteristics.  After  passing  through  the  transi- 
tion beds  separating  it  from  the  Potsdam  sandstone,  it  assumes  all 
the  qualities  characterizing  dolomite.  It  is  very  hard,  compact,  and 
close-grained,  of  a  grayish-white  color.  Beds  of  flint  or  chert  are 


G72     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

contained  in  all  the  strata,  irrespective  of  geological  position,  differ- 
ing however  considerably  from  the  flint  found  in  the  Galena  lime- 
stone, in  that  they  are  more  regularly  segregated,  forming  layers  by 
themselves,  and  are  not  so  promiscuously  distributed  through  the 
formation. 

The  flint  of  the  Lower  Magnesian  limestone  is  much  whiter  and 
more  liable  to  decomposition  than  that  of  the  Galena.  There  are 
also  frequent  geodes  and  cavities  lined  with  drusy  quartz-crystals, 
which  have  never  been  seen  in  the  Galena  limestone,  but  are  very 
adundant  in  the  Lower  Magnesian.  The  crystals  are  of  many  colors, 
white,  yellow  and  rose  color  predominating,  and  often  affording  beau- 
tiful cabinet  specimens. 

A  good  general  idea  of  the  formation  may  be  obtained  from  the 
following  descriptive  section,  taken  from  a  bluff  at  the  mouth  of 
Green  river,  on  the  Wisconsin,  situated  on  the  N.  W.  qr.  of  Sec.  22, 
T.  7,  R.  4  W.  Upon  the  summit  of  the  bluff,  there  was  considerable 
sandstone  scattered  about,  although  none  could  be  found  in  place.  It 
was  found  in  place  on  the  other  side  of  Green  river  at  about  the  same 
elevation,  consequently  we  may  assume  that  the  top  of  the  bluff  is 
quite  near  the  top  of  the  formation: 

A.  Lower  Magnesian  Limesione. 

feet. 

1.  Slope  of  hill  (to  top  of  vertical  cliff)  composed  of  heavy-bedded,  light-gray, 

Magnesian  limestone;  stratification  quite  regular,  contains  no  flints;  good 
building  stone 23 

2.  Hard,  compact,  heavy-bedded,  light-colored  limestone,  lines  of  stratification  not 

distinct;  full  of  irregular  masses  of  flint,  which  compose  about  half  of  the 
bed;  exposed  in  a  vertical  cliff 33 

3.  Slope  of  hill  covering  limestone,  not  well  exposed 23 

4.  Coarse-grained  limestone,  weathering  irregularly  on  exposed  surfaces,  contain- 
ing a  few  flints  disseminated  through  it,  and  occasional  druses  of  quartz 7 

5.  Gray  limestone,  very  hard  and  compact,  regularly  stratified,  beds  from  one  to 

two  feet  thick,  containing  no  flints 29 

6.  Crystalline,  gray,  magnesian  limestone,  with  a  few  flints  irregularly  dissemin- 

ated; beds  two  feet  thick 9 

7.  Hard,  light-colored  limestone,  crystalline  in  texture,  weathering  but  little  on 

exposure;  beds  about  three  feet  thick;  contains  no  flints 46 

8.  Fine-grained,  straw-colored,  slightly  arenaceous,  magnesian  limestone;  beds 

about  one  foot  thick;  stratification  quite  regular , 20 

9.  Irregularly  bedded,  dplomitic  limestone,  has  sometimes  an  oolitic  structure 26 

10.  Yellow,  arenaceous  limestone,  transition  beds.    The  sand  appears  in  rounded 

grains,  separate  from  one  another,  and  cemented  together  with  lime;  strati- 
fication indistinctly  marked 23 

B.  Potsdam  Sandstone. 

11.  Hard  and  compact  sandstone,  in  beds  from  two  to  four  feet  thick,  unfossiliferous,    20 

12.  Very  coarse-grained,  yellow  sandstone,  weathering  in  rounded  masses;  exhibits 

cross  lines  of  deposition;  is  very  soft  and  friable 18 

13.  Slope  of  hill  probably  covering  sandstone 15 

14.  Steep  slope  of  hill  to  water  in  Wisconsin  river;  this  is  probably  the  place  of  the 

shaly,  argillaceous  layers 58 

Total  thickness  from  water  to  top  of  the  bluff 350 

Total  thickness  of  Lower  Magnesian  exposed 239 


GEOLOGICAL  FORMATIONS. 


673 


FIG.  5. 


The  Lower  Magnesian  is  a  formation  of  extremely  variable  thick- 
ness; the  greatest  known  in  the  Lead  region,  is  about  250  feet;  this, 
however,  is  seldom  seen.  The  country  in  the  vicinity  of  the  above 
section,  and  Sec.  20,  of  T.  11,  K.  2  W.,  are  two  instances  where  the  full 
thickness  prevails.  In  ranges  4  and  6  E.,  south  of  the  river,  the  forma- 
tion is  frequently  as  thin  as  one  hundred  feet,  in  some  localities,  and 
in  others,  only  two  or  three  miles  distant,  it  will  attain  double  that 
thickness.  These  sudden  variations  in  thickness  are  due  to  an  un- 
conformability  between  the  Lower  Magnesian  and  the  St  Peters 
sandstone,  discovered  by  Prof.  T.  C.  Chamberlin,  and  described  in 
another  part  of  this  report. 

The  only  change  from  limestone  that  was  observed  was  some  lay- 
ers consisting  of  a  very  fine  calcareous  shale1  with  some  arenaceous 
layers  and  earthy  matter  interlaminated,  about  three  feet  in  thick- 
ness, which  were  noticed  in 
the  valley  of  Grant  river,  in 
the  E".  W.  qr.  of  Sec.  22,  T. 
4,  R.  4W.  They  were  also 
seen  on  Pigeon  creek,  near 
the  center  of  section  24,  in 
the  same  township;  also  in 
the  quarry  at  Reese's  Mill, 
in  the  N.  E.  qr.  of  Sec.  34, 
T.  4,  R.  4  E.,  in  nearly  the 
same  geological  position, 
near  the  top  of  the  forma- 
tion. 

They  were  not  found  oc- 
cupying this  position  in 
other  localities.  Their  pres- 
ence is  due,  probably,  to 
local  causes  alone,  and  they 
cannot  be  considered  as 
constituent  beds  of  the  for- 


SSCTION  OP  CALCAREOUS  AND  ABENACEOUS  SHALES  AT 

GRANT  KITKB. 

1.  St.  Peters  sandstone.  2.  Turfed  slope.  3.  Lime- 
stone bed.  4.  Calcareous  shales.  5.  Limestone  bed.  6. 
Calcareous  and  arenaceous  shales.  7.  Lower  Magnesian 
limestone. 


1  The  following  is  an  analysis  of  the  calcareous  shales,  by  Mr.  E.  T.  Sweet: 

Silica 17.03 

Alumina  3 . 56 

Sesquioxide  of  iron 1 .51 

Carbonate  of  lime 42.14 

Carbonate  of  magnesia 34.56 

Water 1.28 


100.08 


Wis.  SUR.— 43 


674: 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


Fm>  6< 


mation.  About  a  quarter  of  a  mile  east  of  the  preceding  locality,  on 
the  opposite  side  of  Grant  river,  some  of  the  thin  layers  of  the 
Lower  Magnesian  are  slightly  folded  and  bent,  and  are  underlaid 
by  other  and  heavier  beds  which  are  undisturbed.  Their  horizon 
is  a  little  higher  than  the  arenaceous  shales,  probably  near  No. 
2  or  3  of  the  preceding  section.  These  flexures  are  probably  due 
to  a  slight  lateral  or  horizontal  pressure,  exerted  during  the  so- 
lidification of  the  rock,  which  either  did  not  extend  to  the  under- 
lying layers,  or 
which,  by  their 
greater  compactness, 
they  were  able  to 
resist.  The  level 
upper  surface  of  the 
lower  beds  (4),  ex- 
cludes the  idea  of 
unconf  or  inability. 
Fig.  6  is  a  section 
taken  at  this  locality. 
At  the  Welsh  Mill, 

T  Kiver 

in   Iowa    county,   a 
short  distance  north 

a    .  T  SECTION  OF  CURVED  STRATA  AT  GRANT  RIVER. 

or  the  quarter  post 

.    0  -1  1.  St.  Peters  sandstone.    2.  Slope  of  hill  unexposcd.    3.  Curved 

of    SeCS.    18    and    19,      strata  of  limestone.    4.  Heavy-bedded  limestone.    5.  Slope  of  hill 


T.  4,  K.   2  E.,  is  a 

somewhat  anomalous  occurrence  of  the  Lower  Magnesian,  as  shown 

in  Fig.  7. 

FIG.  7. 


SKETCH  OF  LOWER  MAGNESIAN  LIMESTONE  AT  THE  WELSH 
1.  Quarry.    2.  Curved  strata  of  limestone.    8.  West  branch  of  Pecatonica. 

The  Lower  Magnesian  appears  here  on  the  south  side  of  the  stream, 
for  a  distance  of  about  a  quarter  of  a  mile.  It  seems  to- have  under- 
gone a  slight  upheaval  subsequent  to  its  deposition.  The  stream 


GEOLOGICAL  FORMATIONS.  675 

flowing  over  the  sloping  beds  of  the  formation  has  here  a  consider- 
able fall,  which  has  been  utilized  as  a  water  power. 

Paleontology.  The  Lower  Magnesian  limestone  is  characterized 
by  the  extreme  rarity  of  its  organic  remains.  Indeed,  it  is  believed, 
that  up  to  the  period  of  this  survey,  no  fossils  whatever  have  been 
reported  from  the  formation  in  this  portion  of  the  state.  During  the 
summer  of  1873,  several  places  were  discovered  which  establish  their 
existence  beyond  a  doubt.  The  fossils  are  usually  found  imbedded  in 
the  drusy  quartz,  with  which  the  formation  abounds,  arid  usually  in 
the  form  of  casts.  Some,  however,  have  been  found  in  the  limestone. 

From  several  localities,  the  following  are  selected,  because  fossils 
are  more  readily  found  there  than  elsewhere: 

(1)  The  S.  W.  qr.  of  the  S.  W.  qr.  of  Sec.  4,  T.  5,  E.  5  E.,  on  the 
southwestern  slope  of  the  hill  near  the  creek. 

(2)  The  S.  W.  qr.  of  Sec.   12,  and  the  N.  W.  qr.  of  Sec.  13,  T.  5, 
R.  4  W. 

ST.  PETERS  SANDSTONE. 

Geological  Boundaries.  The  formation  known  by  the  above  title 
in  the  geological  reports  of  Io\va,  Minnesota,  Illinois  and  Wisconsin, 
wras  formerly  frequently  designated  as  the  Upper  Sandstone,  in  contra- 
distinction to  the  Lower,  or  Potsdam.  It  is  thought  best  on  account 
of  uniformity,  to  adhere  to  the  present  name.  It  is  found  in  the  val- 
leys of  the  Grant,  Platte  and  Pecatonica  rivers,  and  their  tributaries; 
and  in  Green  county,  it  forms  the  valley  of  the  Sugar  river  and  its 
branches,  this  valley  being  in  many  places  as  wide  as  that  of  the  Mis- 
sissippi. North  of  the  dividing  ridge  it  is  found  about  the  head- 
waters of  the  streams  which  flow  into  the  Wisconsin,  having  its 
northern  outcrop  usually  within  two  or  three  miles  of  the  river,  and 
as  far  east  as  Boscobel,  forming  a  portion  of  the  bluffs  which  inclose 
the  river  valley. 

Lithological  Characteristics.  The  formation  differs  from  the 
Potsdam  sandstone,  in  that  it  contains  no  beds  of  limestone  or  shales 
interstratified  with  it,  but  presents  at  any  given  locality  a  homogene- 
ous structure  through  its  entire  thickness.  Its  color  varies  from  snow 
white,  through  all  shades  of  yellow,  to  a  very  dark  red,  and  in  texture, 
from  friable  crumbling  sand,  to  compact  and  fine-grained  stone.  Be- 
neath the  microscope  the  particles  of  sand  appear  rounded  and  water- 
worn.  The  same  color  and  texture  usually  exist  through  the  entire 
thickness  at  any  given  place. 

The  St.  Peters  formation  frequently  impresses  upon  the  surface  of 
the  country  an  appearance  of  terraces,  although  no  true  terraces,  such 


670  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

as  are  formed  in  river  valleys  by  changes  of  level,  have  anywhere 
been  observed.  This  is  most  readily  seen  in  those  districts  where  it 
becomes  the  surface  rock  over  any  extended  portion  of  country. 

About  the  head  waters  of  Grant  river,  in  the  towns  of  Fennimore, 
Lancaster  and  Mount  Hope,  the  country  is  an  undulating  prairie, 
where  the  hills  are  sandstone,  capped  with  a  little  Buff  limestone,  the 
greater  part  of  that  formation  having  been  denuded.  Here  the  St. 
Peters  can  be  seen,  its  upper  beds  jutting  out  in  low  ledges,  which 
may  be  traced  by  the  eye  continuously  for  long  distances,  about  the 

heads  and  sides  of  the  small  valleys. 

„      Q  Such  exposures  are  very  fre- 

quent in  Green  county,  where, 
addition  to  the  continuous 
exposures,  small  hills  are  fre- 
quently seen,  with  flat  tops, 
which  have  been  denuded  near- 
ly down  to  the  St.  Peters.  The 
accompanying  sketch  represents 

SKETCH  or  A  HILL  IN  THE  TOWN  OF  MT.  PLEASANT.  a  Section  01  SUCI1  an  exposure, 
1.  Soil  and  clay.  2.  Buff  limestone.  3.  St.  Peters  and  is  taken  f  rom  a  tract  of 

eandstone-  country   in   the   town    of    Mt. 

Pleasant,  in  Green  county,  lying  about  the  little  Sugar  river.  The 
characteristics  are  the  cliff  exposure  at  A,  the  steep  slope  of  the 
hill  from  A  to  B,  and  the  table  land  of  Buff  limestone  covered  with 
soil  at  C. 

The  varying  hardness  of  the  upper  bed  of  the  St.  Peters,  some 
portions,  especially  the  white,  being  quite  soft  and  friable,  and 
others  nearly  as  hard  as  quartzite,  due,  perhaps,  to  its  greater  or  less 
impregnation  with  iron,  appears  to  have  caused  an  unequal  resistance 
to  disintegration,  which  has  resulted  in  the  formation  of  Knobs, 
as  they  are  called.  They  are  isolated  pillars  of  sandstone,  which  shoot 
up  in  picturesque  castellated  forms,  frequently  exposing  the  entire 
thickness  of  the  formation,  and  forming  very  conspicuous  objects  in 
the  landscape.  They  are  chiefly  found  north  of  the  dividing  ridge, 
about  the  tributaries  of  the  Wisconsin.  The  following  are  the  most 
remarkable  instances: 

(1)  The  Knobs,  situated  at  the  K  W.  cor.  of  Sec.  21,  T.  7,  R.  4 
E.     They  are  two  conical  hills  of  sandstone,  forming  the  termination 
of  a  ridge  extending  out  from  the  west.     They  exhibit  the  full  thick- 
ness of  the  formation,  which  is  here  about  100  feet. 

(2)  Castle  Rock,  situated  in  the  southwest  corner  of  the  town  of 
Blue  River.     There  are  here  two  very  high  and  precipitous  hills  of 


GEOLOGICAL  FORMATIONS. 

sandstone,  about  250  feet  higher  than  the  stream  which  flows  alono- 
their  base. 

(3)  Pine  Knob,  on  Otter  creek,  S.  E.  qr.  Sec.  9,  T.  7,  K.  2  E. 

(4)  Pompey's  Pillar,  S.  E.  cor.  Sec.  13,  T.  7,  K.  1  E.     This  is  one 
of  the  most  picturesque  and  precipitous  of  all. 

The  peculiarity  of  the  hardness  of  the  upper  beds  has  proved  of 
great  assistance  in  tracing  the  outlines  of  the  formation,  in  determin- 
ing its  thickness,  and  detecting  irregularities  in  the  surface  contour. 

Ripple-marks  on  the  sandstone  were  only  found  at  one  locality.  It  is 
at  a  quarry  in  the  S.  W.  qr.  of  Sec.  3,  T.  2,  E.  5  E.,  at  the  grist-mill 
near  the  mouth  of  Whiteside's  creek;  the  top  of  the  sandstone  being 
about  25  feet  above  the  water.  The  sandstone  is'  very  irregularly 
bedded  in  thin  layers,  with  many  cross  lines  of  deposition,  and  the 
upper  beds  contain  many  hollow  concretions  of  iron  and  sand.  The 
ripple-marks  were  very  plainly  seen  on  some  of  the  layers  by  the  side 
of  the  road,  and  were  very  regular,  parallel  and  well-defined. 

The  St.  Peters  sandstone  differs  very  much  in  its  thickness  in  dif- 
ferent localities,1  although  this  does  not  appear  to  be  the  case  so  much 
in  the  Lead  region  as  near  the  northern  outcrop  of  the  formation,  where 
it  is  in  some  places  as  thin  as  40  feet,  and  in  others,  not  more  than  a 
mile  or  two  distant,  it  is  100,  or  even  150,  feet  thick,  and  seemingly 
depends  on  the  varying  thickness  of  the  underlying  Lower  Magnesian 
limestone.  The  layers  consist  of  subordinate  parts  of  very  various 
lamination,  dipping  in  various  directions. 

Many  instances  were  seen  of  the  varying  thickness  of  Lower  Mag- 
nesian and  St.  Peters  sandstone,2  from  which  the  following  are  se- 
lected: 

(1)  In  the  S.  E.  qr.  of  Sec  26,  T.  8,  E.  1  E.,  is  a  dry  run  in  which 
the  Potsdam  is  seen  in  outcropping  cliffs;  passing  above  the  top  of 
this,  a  clay  soil  sets  in,  which  indicates  the  place  of  the  Lower  Mag- 
nesian, although  it  is  not  seen.     Next  the  St.  Peters  is  seen  in  bold 
cliffs  120  feet  high;    the  distance  from  the  lower  bed  of   the  St. 
Peters  to  the  top  of  the  Potsdam  being  nowhere  over  100  feet. 

(2)  In  the  S.  W.  qr.  of  Sec.  13,  T.  7,  E.  4  W.,  the  St.  Peters  has  a 
thickness  of  150  feet,  of  which  the  upper  15  feet  consist  of  a  soft, 
white,  friable  sand,  in  which  the  usual  concretions  and  impregnations 
of  iron  are  wanting.     This  is  underlaid  by  20  feet  of  yellow  sand- 
stone, and  this  again  by  a  very  dark  red  sandstone. 

(3)  In  the  K  E.  qr.  of  Sec.  29,  T.  8,  E.  2  W.,  the  Lower  Magnes- 
ian limestone  is  just  100  feet  thick,  and  the  St.  Peters  sandstone 
150  feet. 

1  See  page  673.  f  See  page  673. 


678 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


(4)  In  the  S.  E.  qr.  of  Sec.  8,  T.  7,  R.  2  W.,  the  Lower  Magnesian 
is  200  feet,  and  the  St.  Peters  100  feet  thick,  its  upper  surface  being 
nearly  horizontal;  both  formations  appear  to  have  about  their  average 
thickness. 

(5)  In  the  S.  E.  qr.  of  Sec.  2,  T.  6,  R.  3  W.,  the  sandstone  is  about 
70  feet  thick,  and  the  Trenton  limestones  about  50. 

There  are  several  new  localities  which  were  examined  in  1874, 
where  slight  upheavals  of  the  formation  appear  to  have  taken  place. 
The  most  marked  example  of  this,  known  as  Red  Rock,  is  situated  in 
the  valley  of  the  Pecatonica,  in  T.  2,  R.  4  E.  The  sandstone  emerges 
from  the  river  near  the  center  of  Sec.  20.  It  reaches  it  greatest  ele- 
vation near  the  quarter-post  of  Sees.  17  and  18,  where-  it  has  a  thickness 
of  over  100  feet,  and  disappears  again  below  the  river  in  the  S.  E.  qr. 
of  Sec.  7.  The  average  width  of  the  exposure  is  about  half  a  mile. 
It  also  extends  up  the  valley  of  a  small  creek  as  far  as  the  center  of 
Sec.  8.  This  exposure  covers  about  one  and  a  half  square  miles.  The 
following  section  (Fig.  9)  through  the  railroad  cut  at  this  place 
illustrates  the  upheaval: 

FIG.  9. 


UPHEAVAL  OP  ST.  PETERS  SANDSTONE  AT  RED  EOCK. 

In  the  northeast  part  of  T.  3,  R.  5  E.,  there  is  an  upheaval  of  sand- 
stone, beginning  at  the  creek  which  flowrs  nearly  due  west,  south  of 
Sees.  11  and  12.  The  disturbance  continues  north  for  some  distance, 
as  the  whole  ridge  between  this  creek  and  the  one  next  north  of  it 
lies  in  the  sandstone  as  far  north  as  the  Pecatonica  river,  in  T.  4,  R.  5 
E.  The  thickness  of  the  sandstone  is  here  so  great  that  it  is  hardly 
probable  that  it  has  its  normal  position.  A  third  disturbance,  and  the 
last  which  wrill  be  cited,  is  in  T.  2,  R.  6  E.  The  sandstone  on  the 
small  branch  in  Sees.  35  and  36  slopes  gently  toward  Skinner  creek, 
which  appears  to  lie  in  a  slight  depression  or  synclinal  valley.  Pas- 
sing over  the  ridge  between  Skinner  and  Jordan  creeks,  a  slight  an- 
ticlinal ridge  was  discovered,  by  means  of  observations  on  the  top  of 


GEOLOGICAL  FORMATIONS.  679 

the  St.  Peters,  which  was  exposed  in  numerous  small  dry  runs.  The 
top  of  the  formation  was  found  to  be  thirty  feet  higher  on  the  ridge 
than  at  either  of  the  creeks.  Although  disturbances  of  this  kind  are 
extremely  rare  and  infrequent,  yet,  in  these  instances  the  variations 
from  the  normal  dip  are  too  plain  to  be  mistaken. 

Ores  and  Minerals.  The  St.  Peters  sandstone  has  been  carefully 
examined  to  find,  if  possible,  any  indication  of  openings,  either  ver- 
tical or  flat,  such  as  exist  in  the  Galena  limestone.  No  evidences 
were  seen,  except  occasional  vertical  seams  and  fissures,  which  con- 
tained neither  metallic  matter,  nor  minerals  and  clay,  such  as  are 
found  in  veins,  and  which  probably  have  no  connection  with  the  vein 
system  of  the  Galena  limestone.  The  formation  seems  to  be  also  per- 
fectly destitute  of  organic  remains. 

The  only  indication  of  metal  seen  in  this  formation  is  the  presence 
of  small  concretions  of  sandstone,  cemented  by  a  ferruginous  sub- 
stance. This  is  due  to  the  decomposition  of  iron  pyrites  or  marcasite, 
as  is  proved  by  its  existence  in  various  stages  of  decay.  These  con- 
cretions are  not  confined  to  any  particular  part  of  the  formation,  but 
are  much  more  abundant  in  the  upper  beds.  They  are  frequently  per- 
fectly spherical,  and,  when  they  occur  in  the  dark-colored  sandstone,  are 
often  surrounded  by  a  white  ring,  about  half  an  inch  in  width,  from 
which  the  coloring  matter  seems  to  have  been  absorbed.  They  have 
been  noticed  with  more  or  less  frequency  in  various  places,  but  were 
found  most  abundantly  in  the  road  near  the  center  of  Sec  3,  T.  1,  R.  6 
E.  Another  place  was  observed  where  the  concretions  were  wanting, 
and  their  place  had  been  supplied  by  a  different  salt  of  iron;  it  was  in 
the  S.  E.  qr.  of  Sec.  25,  T.  1,  R.  9  E.,  at  the  junction  of  the  Buff  lime- 
stone and  St.  Peters,  The  lower  bed  of  the  former  is  full  of  irregular 
cavities,  and  small  round  holes  about  one-fourth  of  an  inch  in  diameter. 
The  upper  bed  of  the  sandstone  is  colored  green  by  some  salt  of  iron, 
and  in  it  is  a  seam  of  greensand  and  ferruginous  matter.  It  is  a  pe- 
culiarity of  this  formation  that  the  stone  hardens  on  exposure  to  the 
weather.  In  examining  any  natural  exposure,  it  is  found  to  consist 
of  an  outer  indurated  shell,  and  an  inner  and  softer  sandstone.  This 
is  a  valuable  quality,  causing  it  to  be  easily  quarried  and  dressed,  and 
enabling  it  afterward  to  withstand  the  influences  of  the  weather.  In 
addition  to  this,  it  is  easy  to  find  almost  any  color  that  may  be  de- 
sired. Numerous  quarries  exist  in  the  vicinity  of  Mineral  Point, 
furnishing  a  white  and  yellowish-red  stone,  which  is  extensively  used 
in  that  locality. 

Situated  on  Sec.  17,  T.  2,  R.  4  E.,  between  the  villages  of  Darling- 
ton and  Riverside,  on  the  line  of  the  Mineral  Point  railroad,  is  the 


680  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

most  extensive  quarry  that  has  been  opened  any  where  in  this  forma- 
tion. It  is  the  property  of  Mr.  Win.  T.  Henry,  of  Mineral  Point,  by 
whom  it  was  opened  in  the  summer  of  1872.  The  stone  in  this  quarry 
is  of  two  colors,  both  a  very  dark  red,  but  one  somewhat  lighter  in 
color  than  the  other.  It  very  closely  resembles  the  Lake  Superior 
sandstone  in  color,  and  is  by  far  the  handsomest  building  stone  that 
has  come  under  our  observation  in  the  Lead  region.  The  railroad 
passes  through  the  hill,  so  that  the  stone  can  be  loaded  directly  from 
the  quarry  on  the  cars.1 

TRENTON  (BUFF  AND  BLUE)  LIMESTONES. 

Geographical  Boundaries.  It  will  not  be  necessary  to  enter  into 
a  detailed  description  of  the  ground  covered  by  this  formation.  It  is 
sufficient  to  say  that  it  is  always  found  between  the  lowest  bed  of  the 
Galena  limestone  and  the  top  of  the  St.  Peters  sandstone,  and  having 
an  average  thickness  of  about  fifty  feet. 

Lithological  Characteristics.  The  Blue  is  remarkable  as  being 
the  purest  limestone  in  the  Lead  region,  and  the  nearest  approach  to 
the  Trenton,  limestone  of  the  eastern  states,  both  in  its  lithological 
and  paleontological  characteristics.  A  very  noticeable  feature  is  its 
marked  division  into  two  parts;  one  very  heavy-bedded,  in  layers  of 
two  or  three  feet  thick,  known  as  the  glass  rock,  which  constitutes  the 
lower  half;  and  the  other,  thin-bedded,  in  layers  of  two  or  three 
inches,  graduating  sometimes  without  much  change  into  the  thin- 
bedded  Galena  limestone  above.  It  is  at  this  point  that  the  stratum 
of  carbonaceous  shale  occurs,  which  is  the  line  of  demarkation  between 
the  Blue  and  Galena  limestones,  and  as  such,  is  an  unfailing  guide. 
It  varies  very  much  in  its  thickness,  being  from  a  quarter  of  an  inch 
to  a  foot  or  more,  but  wherever  a  good  exposure  of  the  two  formations 
is  seen,  it  has  uniformly  been  found. 

The  carbonaceous  shale  attains  its  greatest  thickness  in  the  vicinity 
of  Shullsburg.  At  the  Oakland  level  on  the  S.  W.  qr.  of  Sec.  5,  T. 
1,  R.  2  E.,  it  varies  from  one  to  two  feet; 2  and  at  the  grounds  of  the 

'The  following  is  an  analysis  of  this  stone,  by  Mr.  E.  T.  Sweet: 

Silica 96 . 74 

Alumina 71 

Sesquioxide  of  iron 1-45 

Carbonate  of  lime 1 .24 

Carbonate  of  magnesia 13 

100. 3'2 

5  Prof.  W.  W.  Daniells,  of  Madison,  has  made  the  following  analysis  of  the  shale: 
carbonaceous  matter,  43.60;  carbonic  acid,  0.88;  water,  0.30. 


GEOLOGICAL  FORMATIONS.  681 

Silvertliorn  mine  on  the  JS".  E.  qr.  of  Sec.  31,  T.  2,  R.  2  E.,  it  has  a 
thickness  of  seven  feet,1  affording  in  each  of  these  localities  small  but 
handsome  crystals  of  Galenite,  having  smooth  polished  faces,  which 
is  but  seldom  the  case  with  crystals  of  this  mineral  found  at  other  lo- 
calities in  the  Lead  region. 

The  following  section  taken  from  the  Darlington  quarry  will  give 
a  good  general  idea  of  the  formation.  The  quarry  is  situated  on  the 
N.  E.  qr.  of  Sec.  3,  T.  2,  R.  3  E.: 

Galena  Limestone. 

Ft.   In. 

1.  Soil  and  loose  rock 2 

2.  Yellowish,  hard,  compact  dolomite,  similar  to  the  Buff  on  the  surface,  but 

not  blue  between  the  layers,  evenly  bedded  in  layers  one  foot  thick 6 

3.  Thin  layers  two  to  four  inches  thick 5     . . 

4.  Carbonaceous  shale 2 

Blue  Limestone. 

5.  Thin-bedded,  very  fossiliferous  limestone,  in  layers  from  two  to  five  inches 

thick 3      6 

6.  Heavy-bedded,  dark  blue  limestone,  very  hard  and  compact,  unfossiliferous 

except  in  the  shaly  partings  between  the  beds 2 •     12     . . 

Buff  Limestone. 
1.  Heavy-bedded,  light  blue  limestone,  weathering  to  buff  on  exposure;  beds 

from  4  to  6  feet  thick,  contains  but  few  fossils,  quarry  rock 32 

8.  Thin-bedded,  fossiliferous  limestone,  similar  to  preceding 13     . . 

9;  Unexposed  beneath  bed  of  river  not  less  than 10 

Total  thickness 83      8 

The  Blue  limestone  has  here  a  thickness  of  fifteen  feet  and  six 
six  inches,  and  the  Buff  not  less  than  fifty-five  feet,  which  is  remark- 
able as  being  much  greater  than  was  seen  at  any  other  point.  Its  av- 
erage thickness  does  not  exceed  thirty  feet. 

1  Also  the  following  analysis  of  the  Silverthorn  shale: 

(1)  Carbonaceous  matter,  18.31;  carbonic  acid,  1.85;  water,  0.40. 

(2)  Carbonaceous  matter,  15.76;  carbonic  acid,  0.60;  water,  0.32.    No.  1  of  the  Sil- 
verthorn shale  was  quite  dark  colored,  while  No,  2  was  a  light,  ash-colored  shale. 

The  specimen  from  Oakland  had  been  for  several  years  exposed  to  the  weather. 

2  The  following  is  an  analysis,  by  Mr.  E.  T.  Sweet,  of  the  Glass  rock  from  Mineral 
Point,  corresponding  to  No.  6  of  the  above  section: 

Silica 6 . 160 

Alumina 2.260 

Sesquioxide  of  iron 950 

.   Carbonate  of  lime  85.540 

Carbonate  of  magnesia 3. 930 

Water 930 

Phosphoric  acid 055 

99.875 


682     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

There  exists  at  Mineral  Point,  at  an  elevation  of  about  fifty  feet 
above  the  upper  surface  of  the  Baft'  limestone,  or  quarry  rock,  a  ' 
stratum  of  compact  limestone  several  feet  in  thickness,  which  in  color 
and  texture  closely  resembles  the  lowest  recognized  Blue  limestone, 
and  contains  Strophomena  alternate,  Leptoena  sericea,  Bellerophon 
fiilobatus,  and  some  varieties  of  Orthis,  all  in  great  profusion,  and  all 
of  them  characteristic  of  the  Blue  limestone  below.  The  strata 
which  separate  them  are  not  exposed. 

It  seems  probable  that  this  upper  stratum  may  correspond  to  Xo. 
5  of  the  preceding  section;  that  Nos.  6  and  7  are  the  unexposed  beds 
at  Mineral  Point;  and  that  Nos.  8  and  9  of  the  Darlington  section 
represent  the  Blue  and  Buff  limestones  at  Mineral  Point.  The  rela- 
tions of  the  two  principal  fossiliferous  strata  are  not,  however,  fully 
apparent  in  the  Lead  region,  nor  does  the  upper  one  seem  to  be  of 
constant  occurrence,  whereas  the  lower  one  is  universally  recognized 
in  Iowa,  La  Fayette  and  Grant  counties. 

East  of  range  three  east,  the  presence  of  the  Blue  limestone  is  no- 
where so  clearly  marked  as  west  of  this  line.  It  is  usually  recog- 
nized by  the  outcropping  of  a  quantity  of  highly  fossiliferous  frag- 
ments, scattered  through  the  soil,  having  a  worn  and  bleached  appear- 
ance. East  of  range  three  the  fossiliferous  Blue  limestone  was  not 
found.  It  is  replaced  by  a  yellowish  limestone,  containing  but  very 
few  fossils,  and  in  all  respects  similar  to  the  Buff  limestone.  The 
thickness  between  the  Galena  limestone  and  St.  Peters  sandstone 
remains  as  usual,  about  fifty  feet. 

There  are  two  exceptions  to  the  foregoing  general  statement.  A 
short  distance  south  of  the  center  of  sec.  18,  T.  1,  R.  6  E,  the  Blue 
limestone  reappears  in  its  full  thickness,  with  all  its  characteristic 
fossils,  but  only  covers  a  small  area  of  ground. 

The  second  exception  is  situated  in  the  town  of  Mt.  Pleasant,  in 
Green  county,  in  the  S.  E.  qr.  of  Sec.  11,  T.  3,  R.  7  E.  It  is  known 
as  the  Marble  Quarry,  so  named  on  account  of  the  fine,  polish  which 
may  be  given  to  the  stone.  The  Blue  limestone  has  here  the  same 
thickness,  both  of  the  thin  and  thick  beds,  as  in  the  western  part  of 
the  Lead  region.  All  the  characteristic  fossils  are  present,  and  in 
short,  it  presents  all  the  usual  lithological  appearances.  It  appears 
to  have  been  deposited  in  a  basin-shaped  depression,  as  the  top  of  the 
St.  Peters  was  found  to  be  much  lower  here  than  any  where  in  the 
vicinity.  Although  separated  many  miles  from  any  other  outcrop  of 
the  Blue  limestone,  it  is  evident  that  it  w#s  deposited  under  the  same 
conditions,  as  in  other  localities.  It  has  been  used  here  for  burning 
lime,  of  which  it  always  makes  a  good  article.  Some  small  pieces 


GEOLOGICAL  FORMATIONS. 


683 


have  been  polished  for  paper  weights,  and  other  small  ornaments.  It 
takes  a  high  polish,  equal  to  marble,  although  large  pieces  cannot  be 
obtained. 

One  other  bed  has  been  observed,  not  mentioned  in  the  descriptive 
section.  It  is  the  line  of  demarkation  between  the  Buff  limestone 
and  St.  Peters  sandstone.  It  consists  of  a  greenish  blue  clay,  usually 
from  one  to  two  feet  thick.  The  clay  is  very  finely  laminated,  and 
consists  of  argillaceous  and  calcareous  matter.  It  might  be  valuable 
as  a  marl,  were  there  not  so  much  of  the  same  constituent  parts  in 
the  surrounding  soil,  as  to  make  its  application  superfluous.  It  is 
not  a  bed  of  invariable  occurrence,  but  it  has  been  seen  in  so  many 
localities,  over  a  great  extent  of  country,  that  it  may  be  regarded  as  a 
constituent  bed  of  the  formation. 

Ores  and  Minerals.  The  Blue  and  Buff  limestones  are  the  low- 
est in  which  any  ores  are  found  in  sufficient  quantities  to  repay  min- 
ing, and  the  northern  and  eastern  parts  of  the  region  in  the  vicinity 
of  Mineral  Point,  Linden.  Dodgeville,  Highland,  Centerville,  Mifflin, 
and  the  Crow  Branch  Diggings  are  the  most  remunerative.  It  is  not 
to  be  inferred  from  this  that  the  formation  is  barren  in  the  southern 
and  western  parts,  but  rather  that  it  lies  so  deep  that  it  has  not  yet 
been  reached  in  the  present  system  of  mining. 

Large  bodies  of  lead  ore  have  from  time  to  time  been  taken  from 
this  formation,  but  it  seems  to  be  more  especially  productive  of  zinc, 
both  as  carbonate  and  sulphuret.  At  present  the  zinc  furnished  from 
the  localities  above  mentioned  is  chiefly  derived  from  it.  For  statis- 
tics of  this  product,  the  reader  is  referred  to  the  latter  part  of  this 
report,  chapter  IV. 

Organic  remains  are  found  in  the  greatest  profusion,  and  in  a  very 
fine  state  of  preservation,  the  rock  in  many  places  being  entirely  com- 
posed of  them.  In  the  Buff  limestone  the}7  usually  occur  as  casts. 
Without  particularizing,  reference  is  made  to  the  general  list. 

GALENA  LIMESTONE.  » 

Geographical  Boundaries.  This  formation  is  by  far  the  most  im- 
portant in  respect  to  its  metallic  wealth  of  all  which  we  have  to  con- 
sider. In  it  are  contained  all  the  mines  of  the  southern  and  western 
parts  of  the  Lead  region,  and  whenever  mining  has  been  carried  on 
in  the  underlying  Trenton  limestones,  lead  is  usually  present  in  the 
overlying  Galena. 

1  In  describing  this  formation  the  term  "  Galena  limestone,"  used  in  other  reports,  has 
been  adhered  to  in  this,  to  prevent  the  confusion  arising  from  several  names  for  the  same 
thing,  although  strictly  speaking  it  is  a  dolomite. 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


The  Galena  limestone  is  the  prevailing  surface  rock  in  the  Lead 
region.  Its  northern  outcrop  conforms  closely  to  the  main  water- 
shed, being  parallel  to,  and  always  within  a  few  miles  north  of  it. 
Its  surface  area  is  given  as  follows,  for  each  range  in  the  Lead  region : 


Range  1  West, 
2 
3 
4 
5 
6 


176  sq.  i 

iiiles. 

Rar 

ge  1  Ea 

st, 

137 

2 

84 

3 

94 

4 

108 

5 

45 

6 

-  190  sq.  miles. 
179 

-  189 
164 

-  103 
144 


644  +  969  =  1,613. 


969 


For  a  more  particular  exposition  of  the  surface  covered  by  this 
formation,  reference  is  made  to  the  maps  accompanying  this  report. 

Lithological  Characteristics.  The  Galena  limestone  is  almost  in- 
variably a  very  compact,  hard,  crystalline  rock,  of  a  yellowish  gray 
color,  with  numerous  small  cavities,  sometimes  filled  with  a  softer 
material,  and  sometimes  lined  with  small  crystals  of  calcite.  The 
upper  portion  is  usually  thick-bedded  and  free  from  flints,  the  layers 
being  from  one  to  four  feet  thick,  while  the  lower  portion  almost  in- 
variably consists  of  several  feet  of  layers  from  one  to  two  inches  thick. 
Good  exposures  of  parts  of  this  formation  are  frequently  to  be  met 
with;  it  may  be  seen  in  cliffs  and  ledges  on  nearly  all  the  streams  in 
the  Lead  region.  It  always  weathers  irregularly  in  these  natural  ex- 
posures, leaving  the  surface  full  of  small  cavities  due  to  the  removal 
of  the  softer  parts. 

The  formation  is  characterized  by  layers  of  flints  which  however 
are  not  constant  in  their  occurrence  in  the  same  beds  at  different  local- 
ities. In  some  places  there  are  several  beds  of  flints,  which  seem  to 
be  connected  with  the  openings,  and  serve  as  a  guide  to  them,  while 
in  others  they  are  either  entirely  absent  or  occupying  very  different 
geological  positions.  The  flints  are  sometimes  found  in  separate 
layers,  deposited  conformably  in  the  rock,  and  often  in  irregular 
pieces  distributed  through  the  strata.  They  seem  to  be  confined 
principally  to  the  middle  and  lower  parts  of  the  formation,  although 
not  entirely  absent  from  any  part. 

The  general  features  of  the  formation  will  be  more  readily  under- 
stood by  reference  to  the  following  descriptive  section  taken  from  a 
bluff  on  the  Mississippi  river,  situated  on  the  S.  E.  qr.  of  Sec.  28.  T. 
3,  R.  5  W.,  where  the  Potosi  road  leaves  the  valley: 

Feet. 

1.  Heavy-bedded,  Galena  limestone;  hard  and  compact,  showing  a  crystalline  struc- 

ture; stratification  very  regular;  good  building  stone,  contains  Receptaculites .     26 

2.  Thin  bedded,  light  yellow  limestone,  containing  flints  intercalated,  and  in  layers 

between  the  beds 6 


GEOLOGICAL  FORMATIONS.  685 

3.  Beds  of  limestone  three  to  four  feet  thick,  containing  but  few  flints;  good  build- Feet. 

ing  stone 12 

4.  Alternating  layers  of  limestone  and  flints 9 

5.  Beds  of  limestone  18  inches  thick,  separated  by  layers  of  flint  two  inches  thick. .  19 

6.  Heavy-bedded  limestone,  layers  two  feet  thick,  containing  nuraerous  intercalated 

flints,  very  hard  and  compact;  stratification  quite  regular 17 

7.  Very  close-grained  limestone,  in  beds  about  four  feet  thick;  good  for  building 

stone;  contains  no  flints 29 

8.  Slope  of  the  hill  to  water  in  the  Mississippi  river  covering  Galena  limestone 91 

Total  thickness 209 

The  ground  rises  as  it  recedes  from  the  bluff',  so  that  there  is  prob- 
ably an  unexposed  thickness  of  at  least  40  feet  of  Galena  limestone 
above  the  top  of  the  cliff. 

The  Galena  limestone  is  in  many  localities  successfully  quarried  as 
a  building  stone.  This  is  chiefly  the  case  in  the  southern  and  western 
parts  of  the  region,  where  the  Buff  limestone  or  St.  Peters  sandstone 
cannot  be  obtained.  The  chief  objection  to  it  is  the  frequency  of 
cavities  and  soft  places  in  it  which  render  it  difficult  to  dress,  and 
cause  it  to  weather  irregularly.  For  foundations,  or  any  work  where 
beauty  of  finish  is  not  the  chief  object,  it  is  a  good  and  durable  stone. 

Paleontology.  The  organic  remains  of  the  Galena  limestone  are 
quite  abundant,  but  do  not  exist  in  such  profusion  as  in  the  Blue 
limestone.  The  characteristic  fossil  of  the  formation  is  the  Recepta- 
culites  Oweni  or  lead  coral,  which  is  found  indifferently  in  all  parts 
of  the  formation.  Next  in  frequency  are  the  Streptelasma  (Petraia) 
corniculum,  and  som  3  varieties  of  small  Orthis.  The  most  infrequent 
is  the  Maclurea  magna,  which  is  found  in  the  middle  beds  of  the 
formation.  In  the  upper  beds  the  Z,ingulaquadrata  is  quite  frequent, 
and  often  found  in  a  fine  state  of  preservation.  Other  and  more  in- 
frequent fossils  are  the  Pleurotomaria  lenticularis,  Belleroplion  bil- 
obatus,  Orthis  biforata,  and  occasional  Orthocerata. 

CINCINNATI  GROUP. 

Geographical  Boundaries.  This  formation  was  found  to  cover  a 
much  larger  area  of  country  than  had  previously  been  supposed.  It 
appears  in  T.  1,  R.  2  E.,  and  has  an  area  of  about  five  square  miles, 
contained  in  the  following  sections:  21,  22,  23,  24,  25,  26,  27,  28,  34, 
35  and  36.  In  T.  1,  R.  3  E.,  it  is  found  in  Sees.  30  and  31,  covering 
about  one  square  mile.  It  does  not  occur  north  of  T.  1,  on  ranges  2 
and  3  E. 

Near  the  corner  of  Sees.  22,  23,  26  and  27,  T.  1,  R.  2  E.,  the  forma- 
tion attains  an  elevation  of  nearly  600  feet  above  Lake  Michigan;  and 


686  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

from  here  to  Scales  Mound  village  it  forms  a  continuous  chain  of  hills, 
among  which  the  most  noticeable  is  Charles  Mound,  which  is  the 
highest  land  in  the  state  of  Illinois.  This  mound  is  capped  with 
about  50  feet  of  Niagara  limestone,  and  in  one  place  a  quarry  has 
been  opened,  from  which  specimens  of  the  fossil  Favosites  favosa 
have  been  obtained. 

The  average  dip  of  the  strata,  in  the  vicinity  of  Scales  mound  is 
about  22  feet  per  mile  in  a  southwesterly  direction,  with  indications 
that  it  is  not  perfectly  uniform  but  slightly  undulating  as  represented  in 

FIG.  10. 


SECTION  FROM  SCALES'  MOUND  TO  THE  STATE  LINE. 
1  Cinncinnati  Group.    2  Galena  Limestone. 

The  Cincinnati  group  next  appears  about  the  Platte  Mounds,  in  the 
southern  part  of  T.  4,  R.  1  E,  and  the  northern  part  of  T.  3,  R.  1 
E.  In  T.  4,  E.  1  E.,  it  is  found  in  Sees.  31,  32,  33,  34,  35,  36,  cov- 
ering an  area  of  nearly  three  square  miles,  and  reaching  an  elevation 
of  1,140  feet  above  the  sea. 

The  formation  also  exists  in  its  full  thickness  at  the  Blue  Mounds, 
but  exposures  of  it  either  natural  or  artificial  are  seldom  visible; 
some  of  the  clay  which  characterizes  the  lower  part  of  the  formation 
was  found  on  the  Brigham  farm  at  the  East  Mound. 

No  exposure  of  this  formation  was  found  at  these  localities.  la 
passing  over  the  gradual  slope  of  the  mounds  it  is  impossible  to  dis- 
tinguish any  boundary  line  between  the  Cincinnati  group  and  the  un- 
derlying Galena  limestone,  such  as  is  seen  on  the  level  table  land 
south  of  Shullsburg,  which  has  been  formed  by  the  denudation  of  the 
soft  shales  which  the  harder  limestone  has  to  a  great  extent  escaped. 
The  line  of  demarkation  between  the  shales  and  the  overlying  Niag- 
ara limestone,  is  well  defined  at  the  West  Platte  Mound  on  all  sides 
by  the  very  marked  change  from  the  steep  slope  of  the  limestone  to 
the  comparatively  gentle  one  of  the  shales.  On  the  north  side  of 
this  mound,  ledges  of  the  Niagara  limestone  may  be  seen  in  place 
almost  to  the  bottom  of  the  formation. 

The  Cincinnati  group  was  also  found  covering  about  seven  square 
miles  of  country,  about  the  Sinsinawa  Mound,  in  the  following  sec- 
tions: 1,12,  13,  14,  24,  25,  26,  35,  36,  T.  1,  E.  2  W.  Sees.  6,  7,. 8,  16. 
17,  18,  19,  20,  29,  30,  31,  T.  1,  E.  1  W.,  extending  north  from  the 


GEOLOGICAL  FORMATIONS.  687 

Sinsinawa  Mound,  as  far  as  Jamestown.  Nearly  all  the  mines  on 
the  ridge  north  and  east  of  Fairplay  are  sunk  through  the  lower  part 
of  the  Cincinnati  group,  and  good  specimens  of  Nucula,  fecunda, 
may  often  be  found  in  the  dirt  thrown  out  of  the  shallow  holes,  when, 
the  clay  has  not  been  covered  again  by  the  refuse  of  deeper  workings. 

Lithological  Characteristics.  The  strata  of  the  Cincinnati  group 
are  very  regularly  and  conformably  deposited,  and  do  not  exhibit  any 
indications  of  sudden  and  violent  dislocations,  faults,  or  uplifts. 

The  lower  beds  of  the  formation  are  very  finely  laminated,  and  of 
a  dark  blue  color,  in  many  places  becoming  green  and  brown.  The 
upper  layers  are  of  a  yellowish  color,  and  more  or  less  calcareous  and 
silicious. 

The  lower  and  middle  members  of  the  group  split  readily  and  with 
a  very  smooth  face,  but  the  upper  layers,  though  quite  thin-bedded, 
present  a  rough  and  uneven  appearance.  This  group  nowhere  presents 
beds  of  sufficiently  thick  and  durable  stone  for  building  purposes. 
Only  one  place  was  noticed  where  an  attempt  had  been  made  to  quarry 
this  rock;  it  had  been  abandoned  as  impracticable,  after  a  small 
amount  of  work  had  been  done. 

Where  undisturbed,  this  group  has  a  thickness  of  about  125  feet. 
This  is  the  case  only  on  the  mounds,  which  are  still  capped  with  the 
Niagara  limestone,  as  in  all  other  places  it  has  been  more  or  less  re- 
moved by  denudation. 

There  is  nowhere  a  good  natural  exposure  of  the  formation.  The 
rocks  throughout  the  group  offer  so  little  resistance  to  the  weather 
that  they  do  not  appear  in  rugged  cliffsy  such  as  are  seen  in  all  the 
formations  which  underlie  them,  but  usually  in  gently  undulating 
hills.  The  best  exposure  is  the  one  in  the  cut  of  the  Illinois  Central 
railroad,  near  Scales  Mound  Station,  of  which  a  very  accurate  section 
has  already  been  given  in  Prof.  Hall's  report.  It  is  much  more  accu- 
rate than  can  now  be  obtained,  as  the  weather  has  since  then  so  de- 
composed the  friable  shales  that  only  a  few  feet  of  the  lower  beds  are 
now  visible,  as  they  were  originally  presented.  As  a  general  guide 
to  the  formation,  we  take  the  liberty  of  reproducing  it: 

Ft.    In. 

1.  Greenish  shale,  with  alternations  of  calcareous  and  silicious  layers,  a  few 

inches  in  thickness 7      8 

2.  Green  silico-calcareous  and  argillaceous  shales 11      6 

3.  A  silico-calcareous  or  niagnesian  band 3 

4.  Greenish  shale  as  above 12 

5.  Concretionary  layer,  1  to  3  inches 3 

6.  Shale  with  Lingula 6 

7.  A  layer  filled  with  a  small  Nucula,  and  known  as  the  Nucula  bed,  4  to  8 

inches 8 


688  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

8.  A  calcareous  band  cut  by  open  joints  or  fissures,  into  which  the  materials  of   Ft-   In. 

the  layer  above  have  penetrated , 4 

9.  Dark  olive  shales,  finely  laminated  and  destitute  of  fossils 3      4 

10.  Nucula  bed,  similar  to  the  above,  4  to  6  inches 6 

Total  thickness  exposed 42      6 

A  noticeable  feature  of  the  two  Nucula  beds,  which  are  the  lowest 
of  the  series,  is  that  the  floor  of  each  is  a  thin  seam  of  pyrites  of  a 
nodular  and  crystalline  form  which  rests  on  the  bed  below.  This 
was  the  only  metalliferous  indication  noticed  in  the  formation,  and  it 
did  not  seem  to  exist  in  great  abundance. 

The  beds  of  Galena  limestone  which  underlie  this  formation  are 
quite  regularly  stratified  in  beds  about  six  inches  thick.  In  the  west 
end  of  the  cut,  the  beds  are  perfectly  horizontal  on  a  course  !N".  55°  "W. 
On  a  course  at  right  angles  to  this,  the  dip  was  found  to  be  about  50 
feet  per  mile  on  a  S.  W.  course.  It  is  probable,  however,  that  this  is 
only  a  local  dip. 

Nothing  of  a  metallic  nature  was  discovered  in  the  formation,  ex- 
cept a  few  small  seams  of  marcasite  in  the  lower  beds. 

The  best  localities  for  obtaining  fossils  from  this  formation  are  on 
the  sides  of  the  mounds,  where  the  water  has  partly  removed  the 
turf  and  soil,  and  formed  gullies  which  are  filled  with  broken  frag- 
ments of  the  different  beds.  Among  these  may  be  mentioned  the 
S.  E.  qr.  of  Sec.  22,  T.  1,  R.  2  E.,  near  what  is  known  as  the  Gratiot 
place.  The  lower  beds  abound  with  shells  of  the  Nucula  fecunda; 
the  middle  ones  with  Rhynchonella  increbescens,  Strophomena  alter - 
nata,  and  stems  of  Chcetetes.  The  upper  beds  contain  a  few  Orthoce- 
rata,  but  they  are  infrequent. 

The  lower  beds  of  the  Cincinnati  group  have  been  exposed  in  some 
old  diggings  in  the  N".  E.  qr.  of  sec.  2,  T.  3,  R.  1  E.,  on  the  road  near 
the  Burris  place.  Specimens  of  the  Nucula,  and  other  shells  charac- 
teristic of  the  lower  beds  were  here  found  in  great  profusion  and  per- 
fection. 


ATE.XXX 


TUB  MllM-AI'ICKRl.lTHI>.<r  KKUK.CV 


VIEW  OF  BLUFFS    ON  THE    MISSISSIPPI. 


THE  LEAD  REGION.  689 


CHAPTER  IT. 
THE    LEAD    KEGIO2T. 

Boundaries  and  Area.  In  Wisconsin,  the  Lead  region  may  be 
said  to  be  bounded  on  the  north  by  the  northern  outcrop  of  the  Ga- 
lena limestone,  running  parallel  to  the  main  watershed  from  the  Mis- 
sissippi to  the  Blue  Mounds,  as  already  described;  on  the  west  by  the 
Mississippi  river;  on  the  south  by  the  state  line;  on  the  east  by 
Sugar  river.  These  limits  include  all  of  the  Lead  region  which  har, 
ever  been  productive,  as  well  as  much  that  has  never  as  yet  proved  so. 
The  area  thus  included  which  has  been,  or  may  hereafter  become  pro- 
ductive, is  necessarily  that  of  the  Galena  limestone,  which  is  about 
1,776  square  miles. 

Explanation  of  Mining  Terms.  For  the  enlightenment  of  the 
readers  of  this  report,  who  are  unfamiliar  with  mining  terms,  the 
following  short  explanation  of  expressions  most  frequently  used  in 
the  Lead  region  is  offered. 

Range.  This  is  probably  the  most  indefinite  term  in  use,  and  at 
the  same  time,  one  which  is  universally  applied.  1st.  A  range  de- 
notes a  single,  or  several  parallel  crevices,  containing  useful  ores  or 
minerals;  vertical,  or  approximately  so;  seldom  more  than  a  few 
yards  apart;  sometimes,  but  not  necessarily,  connected  by  quartering 
crevices.  Its  length  may  vary  from  a  few  hundred  feet  to  a  quarter 
of  a  mile  or  more;  in  short,  BO  far  as  the  crevice  or  crevices  have 
been  connectedly  traced,  or  there  is  a  reasonable  probability  of  such 
connection.  Thus,  different  parts  of  the  same  range  often  have  dif- 
ferent names  given  them  before  the  connection  between  them  is 

~ 

proved.  This  is  a  fruitful  source  of  confusion.  3d.  The  term  range 
is  also  applied  to  horizontal  bodies  of  ore,  of  which  there  may  be 
one,  or  several,  superimposed  upon  one  another;  sometimes,  but  not 
necessarily  separated  by  unproductive  layers  of  rock,  limited  in 
length  in  the  same  way  as  a  vertical  range. 

Crevice.     This  term  denotes  a  fissure  in  the  rock,  vertical  or  near- 
ly so,  but  a  few  inches  in  width,  of  indefinite  length,  which  may  or 
may  not  be  filled  with  ores  or  minerals;  when  a  crevice  becomes  very 
small,  less  than  an  inch  in  width,- it  is  called  a  seam. 
Wis.  SUB.  — 44 


690 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


FIG.  11. 


Vein,  is  a  term  little  used;  it  denotes  the  filling  of  ore  and  accom- 
panying minerals,  or  either,  found  in  a  crevice. 

Lode  or  Lead5  are  words  usually  substituted  for  vein;  they  are, 
however,  generally  applied  to  ore  deposits  found  either  in  crevices  or 
openings. 

S  wither,  a  metalliferous  crevice,  making  an  angle  with  the  prin- 
cipal vein  or  lode,  sometimes  called  a  quartering  crevice. 

8  o'clock,  10  o'clock,  etc,  ranges  whose  course  bears  toward  the 
sun  at  those  hours  of  the  day. 

Openings.  They  are  of  two  kinds,  vertical  and  horizontal.  1. 
Vertical  openings  are  known  as  crevice  openings,  which  are  mere  en- 
largements of  the  crevice  in  certain  parts,  these  being  sometimes  co- 
extensive with  the  vein  in  length,  and  sometimes  mere  local  enlarge- 
ments. There  are  in  the  same  crevice  frequently  several  openings, 
situated  one  above  the  other,  separated  by  beds  of  unproductive  rock. 
Crevices  vary  in  width  from  one  to  several  feet ;  when  very  wide  and 
high,  they  are  sometimes  called  tumbling  openings.  2.  Horizontal 

openings  are  large 
irregular  spaces 
between  the  strata 
which  contain  the 
lode.  Such  open- 
ings are  usually 
from  one  to  four 
feet  high,  and  are 
frequently  super- 
imposed upon  one- 
another,  separated 
by  an  unproduc- 

SECTION  OF  OPENINGS  (ideal),  tive  rock    called   a 

A,  Crevice;  B,  Crevice  opening;  C,  Flat  opening;  D  D,  Flat  openings  "cap."    The  "cap" 
connected  "by  E  E,  Pitching  sheets ;  F.  Pocket  with  ore.  „ 

or  one  opening  be- 
ing frequently  the  "  floor  "  of  the  one  above  it. 

Pockets  are  small  irregular  cavities  in  the  strata  in  which  ore  is 
frequently  obtained. 

Chimneys  are  irregularly  shaped  vertical  holes  found  in  crevices; 
sometimes  connecting  openings,  and  at  others  extending  from  the 
surface  of  the  ground  to  some  particular  stratum  of  rock. 

Sheet.  This  is  a  term  usually  employed  to  designate  a  solid  body 
of  ore  exclusive  of  other  minerals  which  may  fill  a  crevice  or  open- 
ing. A  sheet  is  said  to  "  pitch  "  when  it  inclines  considerably  fro  in 
the  perpendicular. 


MINERALOGY. 


691 


Gouge.  This  is  the  soft  rock  or  clay  frequently  found  between  the 
sheet  and  adjacent  wall-rock. 

Bar.  The  term  denotes  a  band  or  belt  of  very  hard  and  unpro- 
ductive rock,  crossing  the  crevices  and  sheets.  In  crossing  a  bar  all 
sheets  become  less  productive,  and  are  sometimes  entirely  lost,  the 
crevices  usually  dwindling  to  mere  seams.  Their  width  varies  from 
a  few  feet  to  many  yards. 

Wash-dirt,  is  the  name  given  to  the  small  ore  as  it  first  comes 
from  the  mine,  mixed  with  small  pieces  of  rock  and  clay. 

Pipe-Clay.  A  light  colored  plastic  clay  frequently  found  in  the 
openings  and  crevices. 

Drift.     An  underground  gallery  or  roadway. 

MIKEEALOGY. 

There  does  not  appear  to  have  been  any  absolute  and  unvarying  order  in  which  the 
minerals  of  the  Lead  region  were  deposited  in  the  mines.  The  following  conclusions 
are  derived  from  the  inspection  of  the  ore  as  it  occurs  in  place  in  the  numerous  mines 
visited,  and  from  the  examination  of  a  great  number  of  specimens;  and  it  is  assumed 
that  when  crystals  of  one  mineral  are  coated  or  covered  with  another,  the  overly- 
ing one  is  the  more  recent.  The  minerals  appear  to  have  been  deposited  in  the  follow- 
ing general  order : 

GALEKITE. 

SPHALERITE. 


DOLOMITE,  CALCITE. 


PTRITE,  MAKCASITE,  CHALCOPYRITE. 
BAUITE. 

CALCITE. 

I 

CERUSSITE,  SMITHSONITE,  MALACHITE,  AZURITE. 

The  order  above  given,  however,  is  subject  to  very  numerous  and  important  excep- 
tions, and  is  more  particularly  applicable  to  crystallized  specimens  than  to  heavy  ore  de- 
posits. Large  bodies  of  ore  frequently  consist  of  galenite,  sphalerite  and  pyrite,  so 
mingled  together  that  no  order  of  deposition  can  be  ascertained. 

In  general  it  appears  that  the  sulphurets  of  the  metals  were  deposited  first,  and  that 
the  carbonates  have  been  generally  if  not  invariably  derived  from  them.  Carbonate  of 
lead  (cerussite),  when  found  crystallized,  always  occurs  in  connection  with  galenite;  and 
carbonate  of  zinc  (Smithsonite)  is  so  frequently  found  graduating  into  the  sulphuret 
(sphalerite)  as  to  leave  but  little  doubt  of  its  origin  from  that  mineral. 

It  seems  not  improbable  that  the  formation  of  the  carbonate  of  zinc  may  even  now 
be  taking  place  in  the  ground  to  quite  a  large  extent;  especially  in  such  deposits  as  are 
not  below  the  water  level,  or  are  only  periodically  submerged.  It  is  a  well  known 
fact  that  the  Drybone  diggings  are  usually  comparatively  free  from  water,  and  that 


092  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

the  zinc  ore  below  the  water  level  is  usually  blende  (sphalerite)  with  but  little  admix- 
ture of  the  carbonate.  As  the  level  of  the  water  in  the  ground  becomes  gradually  lower, 
and  it  is  a  well  known  fact  that  it  does,  the  atmosphere,  together  with  surface  water 
charged  with  carbonic  acid,  is  permitted  to  act  upon  the  blende,  and  a  transformation 
from  the  sulphuret  to  the  carbonate  is  the  result. 

The  association  of  calcite  with  other  minerals  is  such  as  to  indicate  that  it  must  have 
been  formed  in  crystals  during  at  least  two  different  periods.  Stalactites  of  recent  ori- 
gin are  found  in  the  mines,  which  on  being  fractured  show  a  distinct  crystalline  struc- 
ture, and  large  planes  of  cleavage. 

The  following  is  a  list  of  the  minerals  known  to  occur  in  the  Lead  region,  arranged 
according  to  the  system  adopted  by  Prof.  Dana,  in  his  Mineralogy  : 

Sulphur.  Native  sulphur  is  found  but  seldom  in  the  Lead  region;  its  presence  is 
usually  due  to  the  decomposition  of  iron  pyrites.  It  is  usually  found  in  a  pulverulent 
form.  Some  pieces  weighing  as  much  as  an  ounce  were  seen  in  a  cabinet  at  Hazel 
Green,  which  are  said  to  have  been  obtained  from  a  small  sheet  in  some  of  the  Bun- 
come  mines.  It  is  said  to  be  not  uncommon  in  this  vicinity.  Other  localities  where  it 
is  found  are,  Mineral  Point  and  the  Crow  Branch  diggings. 

Bornite.  Variegated  or  Purple  Copper  ore.  Composition:  copper  62.5;  iron  13.8; 
sulphur  23.7.  This  is  quite  a  rare  mineral;  a  few  pieces  have  been  found  in  the  copper 
diggings  near  Mineral  Point;  it  has  never  been  found  here  crystallized,  but  always  mas- 
sive and  in  small  pieces. 

Galenite.  Composition:  lead  86.6;  sulphur  13.4.  This  is  the  only  ore  of  lead  found 
in  sufficient  quantities  to  be  of  economic  value;  it  is  universally  known  in  the  Lead  re- 
gion as  "mineral."  It  frequently  occurs  in  distinct  crystals,  either  as  a  cube  or  some 
modification  of  it.  Octahedral  crystals  are  quite  rare,  but  are  occasionally  found,  espe- 
cially in  the  carbonaceous  shale  of  the  southern  part  of  the  region.  Usually,  however, 
galenite  occurs  massive,  with  a  very  distinct  cleavage.  Freshly  broken  surfaces  have 
always  a  bright  steel  color,  which  speedily  tarnishes  on  exposure,  to  the  air. 

Sphalerite.  Blende  or  Black-jack.  Composition:  zinc,  67;  sulphur,  33.  This  is 
one  of 'the  most  abundant  minerals  in  the  Lead  region,  besides  being  of  great  economic 
value  as  an  ore  of  zinc.  It  is  almost  invariably  found  as  an  associate  vein-mineral  in  the 
horizontal  deposits  of  Lead  ore.  It  is  usually  found  massive  and  compact,  of  a  dark 
brown  or  black  color,  due  to  a  small  portion  of  iron  contained  in  it,  and  more  or  less 
mixed  with  galenite.  The  Lead  region  has  never  afforded  a  perfect  crystal  of  blende, 
although  many  specimens  are  found  with  small  and  imperfect  crystalline  faces.  The 
fractured  surfaces  of  such  specimens  usually  have  a  resinous  luster. 

Pyrite.  Composition:  iron,  46.7;  sulphur,  53.3.  This  is  the  most  common  vein- 
mineral  found  in  the  mines;  it  is  universally  met  with  in  veins,  lodes  or  other  deposits 
of  ore,  and  in  many  cases  impregnates  the  rock  when  all  other  metals  are  absent.  In 
crevices  it  frequently  appears  to  have  been  the  first  mineral  deposited.  It  is  usually 
found  massive,  although  handsome  crystallized  specimens  are  frequently  obtained  from 
the  mines.  In  crystals  it  usually  assumes  some  modification  of  the  cube,  the  octahedron 
being  quite  frequent.  It  also  occurs  in  radiated  and  reniform  masses.  It  has  never  yet 
been  considered  of  any  economic  value  in  the  Lead  region,  and  as  it  is  so  much  mixed 
•with  rock,  it  is  doubtful  if  it  could  be  profitably  separated,  except  by  the  natural  process 
of  disintegration,  to  which  some  varieties  are  liable  when  exposed  to  the  air.  The  Crow 
Branch  diggings  and  the  Linden  mines  afford  large  quantities  and  good  specimens  of 
this  mineral. 

Marcasite.  Composition:  iron,  46.7;  sulphur,  53.3,  or  same  as  pyrite.  The  difference 
between  this  and  the  preceding  is  but  slight,  and  chiefly  due  to  crystalline  structure; 
the  former  belonging  to  the  monometric  and  the  latter  to  the  trimetric  system.  It  is 
somewhat  lighter  colored  than  pyrite,  and  decomposes  more  readily  in  the  air.  It  is 


MINERALOGY. 

quite  a  common  vein- mineral  and  occurs  in  globular  and  cockscomb  shapes.  It  is  abund- 
ant in  the  New  Diggings  district.  It  is  difficult  to  preserve  specimens  of  this  mineral 
longer  than  a  few  months. 

,  Chaleopyrite.  Composition:  copper  S4.6;  iron,  30.5;  sulphur  34.9.  This  is  th? 
principal  ore  of  copper  in  the  Lead  region,  and  is  most  abundantly  found  in  the  vicinity 
of  Mineral  Point.  It  usually  occurs  massive,  frequently  mixed  with  pyrite;  small  and 
indistinct  crystals  are  occasionally  found. 

Hematite.  Composition:  iron,  70;  oxygen,  30.  Impure  arenaceous  varieties  of  this 
mineral  frequently  occur,  nowhere,  however,  sufficiently  rich  or  abundant  to  be  of  any 
economic  value.  It  seems  to  be  chiefly  due  to  the  decomposition  of  pyrite,  and  is  most 
common  as  the  ferruginous  sandstone  concretions  in  the  upper  beds  of  the  St.  Peters. 
It  is  also  frequently  found  as  ocher,  with  other  vein-minerals,  especially  in  the  flat 
openings. 

Oxide  of  3Ianganese.  A  substance  consisting  of  oxide  of  manganese  with  a  little 
oxide  of  iron,  zinc,  and  traces  of  magnesia  according  to  an  analysis  of  Dr.  Bode  of  Mil- 
waukee, is  found  in  crevices  in  the  Trenton  limestone,  in  some  diggings  situated  on. 
Sec.  11,  T.  4,  R.  1  E.  The  mineral  is  as  light  as  cork,  color  brownish- black,  submetallic 
luster  and  streak,  soils  readily,  and  is  infusible.  It  is  very  soft,  and  does  not  occur 
crystallized.  It  has  a  structure  in  thin  parallel  layers  resembling  wood. 

Calamine.  Composition:  silica,  25.0;  oxide  of  zinc,  67.5;  water,  7.5.  Tin's  mineral 
is  of  very  rare  occurrence  in  the  Lead  region.  It  is  found  in  small,  drusy  crystals, 
coating  Smithsomte.  The  crystals  are  very  brittle,  colorless,  and  have  a  vitreous  lustre. 
It  is  found  near  Mineral  Point. 

Barite.  Composition:  sulphuric  acid,  34.33;  baryta,  65.67.  It  occurs  usually  white 
and  massive,  but  sometimes  in  lamellar  and  crested  forms.  The  only  place  where  it 
was  found  in  distinct  crystals  was  in  the  railroad  cut  at  Scales  Mound,  where  it  occurs 
in  small  cavities,  as  small  but  very  perfect  transparent  crystals,  associated  with  dolo- 
mite and  pyrite.  It  is  not  a  very  abundant  mineral,  but  is  found  in  several  of  the  min- 
ing districts,  especially  Dodgeville  and  Mineral  Point.  The  following  is  an  analysis  by 
Mr.  E.  T.  Sweet,  of  a  specimen  from  the  S.  W.  qr.  of  Sec.  6,  T.  5,  R.  3  E.,  on  Van 
Meter's 'survey: 

Silica 2.24 

Alumina 83 

Sesquioxide  of  iron 77 

Water Trace. 

Barite,  sulphate 95.27 

Lime,  sulphate 1 .30 

100.41 


Anglesite.  Composition:  sulphuric  acid  26.4;  oxide  of  lead  73.6.  Traces  of  this 
mineral  are  reported  as  occurring  in  some  of  the  mining  districts,  but  no  specimens 
have  as  yet  been  obtained.  It  probably  originates  from  the  decomposition  of  galenite. 

Calcite.  Composition:  carbonic  acid  44;  lime,  56.  This  is  a  vein-mineral  common 
to  all  the  deposits  of  ore  whether  in  crevices  or  openings.  It  occurs  crystallized  in  modified 
rliombohedrons  and  scalenohedrons.  The  variety  known  as  Dog-tooth-spar  is  a  very 
frequent  form,  especially  in  the  Shullsburg  and  Linden  districts  which  affords  very  hand- 
some cabinet  specimens.  The  Mineral  Point  district  affords  handsome  rhombohedrons, 
and  the  Linden  mine  affords  handsome  twin  crystals  of  calcite  set  on  sphalerite  (blende). 
It  also  occurs  there,  rarely,  as  a  pseudomorph  after  marcasite  and  has  then  a  radiate  or 
divergent  form. 

Dolomite.    Bitter  Spar  or  Brown  Spar.    Composition:  carbonate  of  lime  and  car- 


694:     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

bonate  of  magnesia,  in  slightly  varying  but  nearly  equal  proportions.  It  occurs  occas- 
ionally in  small  rhombohedral  crystals  in  cavities  of  the  Galena  limestone.  The  best  lo- 
cality for  obtaining  cabinet  specimens  is  in  the  railroad  cut  at  Scales  Mound. 

Sraithsouite.  Often  improperly  called  Calamine.  Composition:  carbonic  acid, 
85.18;  oxide  of  zinc,  64.81.  This  mineral,  commonly  known  as  Drybone,  is  one  of 
the  two  ores  of  zinc  found  in  the  Lead  region.  It  is  found  most  extensively  in  the  cen- 
tral and  northern  parts  and  usually  in  connection  with  blende.  It  crystallizes  in 
rhombohedral  forms;  such  specimens  are,  however,  rare.  It  usully  occurs  massive,  hav- 
ing a  structure  similar  to  partially  decayed  bone,  from  which  it  derives  its  common 
name. 

Pseudomorphs,  of  Smithsonite,  after  calcite,  are  sometimes  formed.  They  occur  as 
rhombohedrons,  and  in  the  various  irregular  shapes  in  which  calcite  occurs  in  the  Lead 
region.  Perfect  crystals,  in  which  the  transformation  from  calcite  to  Smithsonite  is 
complete,  are  very  rare.  It  is  much  more  common  to  find  skeleton  crystals,  or  those 
which  have  been  formed  by  the  deposition  of  a  smooth,  light-colored  shell  of  Smithsonite, 
about  a  sixteenth  of  an  inch  thick,  over  all  the  exposed  surface  of  the  calcite,  followed 
by  a  gradual  removal  of  the  crystal  contained  within  the  shell.  The  space  within  the 
shell  is  sometimes  partially  filled  with  Smithsonite,  and  frequently  planes  are  formed 
within,  parallel  to  the  cleavage  planes  of  the  original  crystal.  Pseudomorphs  are  also 
found  in  which  the  imperfect  crystallization  of  sphalerite  is  very  evident.  Smithsonite 
is  also  found  covering  crystals  of  galenite,  which  are  undecomposed. 

Cerussite.  Composition :  carbonic  acid,  16.5;  oxide  of  lead,  83.5.  Cerussite  is  occasion- 
ally fonnd  in  small  pieces,  but  never  in  sufficient  quantities  to  form  an  object  of  mining. 
It  occurs  in  irregular  rounded  pieces  of  a  yellowish  color,  exhibiting  no  crystalline 
structure.  It  has  been  found  near  Mineral  Point,  and  in  former  years  quite  frequently 
at  the  diggings  near  Blue  Mounds. 

Cerussite  is  found  in  small,  irregular,  translucent  crystals  of  a  white  or  light  yellow 
color,  in  the  mine  of  Messrs.  Poad,  Barrett  &  Tredinnick,  near  Linden.  The  specimens 
seen  were  large,  cubic  crystals  of  galenite  coated  with  pyrite,  the  crystals  of  cerussite 
being  formed  on  both  of  these  minerals.  The  specimens  indicate  that  the  crystals  of 
pyrite  had  been  formed,  and  many  of  them  broken  before  the  formation  of  the  cerussite. 

Hydrozincite.  Composition:  carbonic  acid,  13.6;  oxide  of  zinc,  75.3;  water, 
11 .1.  This  is  a  mineral  of  rare  occurrence  in  the  Lead  region.  It  is  found  at  Linden 
and  Mineral  Point  as  a  white,  finely  crystalline,  fibrous  incrustation  on  Smithsonite. 

Malachite.  Composition:  carbonic  acid,  19.9;  protoxide  of  copper,  71.9;  water, 
8.2.  It  is  occasionally  found  in  small  seams  mixed  with  other  ores  of  copper  in  tb.e 
Mineral  Point  copper  mines.  Crystals  or  good  cabinet  specimens  do  not  occur. 

Aznrite.  Composition:  carbonic  acid,  25.6;  protoxide  of  copper,  69.2;  water,  5.2. 
It  occurs  similar  to  malachite,  massive  and  in  seams  associated  with  chalcopyrite.  The 
Mineral  Point  mines  afford  very  beautiful  cabinet  specimens  of  small  rhombohedral 
crystals  of  dark  blue  color. 

PRESENT  CONDITION  OF  THE  MINES  IN  THE  VARIOUS  DISTRICTS. 

In  this  subdivision  of  the  chapter,  it  is  desired  to  present  such  information  in  regard 
to  the  individual  mines  as  has  been  collected  during  the  course  of  the  survey  up  to  the 
time  when  it  became  necessary  to  submit  the  manuscript  for  publication.  This  infor- 
mation has  in  many  cases  been  procured  under  difficulties;  owing  sometimes  to  tem- 
porary suspension  of  mining  operations,  sometimes,  but  not  often,  to  the  reticence  of 
owners,  and  sometimes  to  petty  and  vexatious  hindrances  which  are  best  understood  by 
those  who  have  ever  attempted  to  collect  such  information.  It  has  been  our  aim  per- 
sonally to  inspect  and  visit  all  the  mines  of 'any  considerable  magnitude,  or  possessing 


MINES  — BEETOWN  DISTRICT.  695 

any  features  of  geological  or  mineralogical  interest;  and  in  nearly  all  cases  the  owners 
have  been  found  ready  to  afford  every  facility  for  investigating  and  obtaining  infor- 
mation. 

Mining  is  a  business  in  which  change  is  the  rule  and  not  the  exception,  it  is  therefore 
probable  that  some  changes  may  have  occurred  since  the  commencement  of  the  survey 
which  are  not  here  recorded,  although  it  has  been  our  aim  to  discover  and  incorporate 
them  in  the  following  report.  The  mines  of  the  Lead  region  will  be  considered  under 
separate  districts,  as,  in  fact,  they  are  geographically  distributed. 

The  visitor  in  the  Lead  region  will  constantly  hear  the  terms  "  Brown  rock,"  "  Glass 
rock,"  "  Pipe-clay  opening,"  etc.,  used  by  the  miners  to  designate  the  different  strata 
in  which  they  work  This  would  be  an  advantageous  system,  were  it  not  that  the  sev- 
eral names  are  applied  to  widely  different  strata  by  persons  in  the  several  districts.  The 
term  "  Glass  rock,"  for  instance,  is  indiscriminately  applied  to  all  the  strata  in  the  Buff, 
Blue  and  Galena  limestones.  The  following  section  is  given  as  a  general  guide  in  un- 
derstanding the  relative  position  and  thickness  of  the  strata  and  openings,  to  which  ref- 
erence will  occasionally  be  made  in  the  subsequent  pages.  The  section,  however,  will 
not  be  found  of  universal  application,  but  merely  shows  the  strata  as  their  position  is 
now  understood  by  the  most  intelligent  and  systematic  miners.  In  practice,  the  most 
reliable  plan  for  determining  the  geological  position  of  an  ore  bed  or  mine  is,  to  find  the 
outcrop  of  some  well  defined  horizon  in  the  vicinity,  and  ascertain  the  distance  of  the 
bed  or  mine  above  or  below  it,  after  making  due  allowance  for  the  dip. 

There  are  numerous  openings  occurring  in  all  the  upper  and  middle  beds  of  the  Galena 
limestone,  none  of  which  appear  to  be  found  regularly  hi  all  the  districts.  The  section 
is,  therefore,  confined  to  the  more  persistent  openings  of  the  lower  beds. 

Galena  Limestone. 

Feet. 
Green  rock 4 

Green  rock  opening 3 

Green  rock 12 

Brown  rock 12 

Brown  rock  opening 5 

Brown  rock 8 

Buff  and  Blue  Limestone. 

Upper  pipe  clay  opening 5 

Glass  rock  (Blue  limestone) v  25 

Glass  rock  opening 6 

Buff  limestone 12 

Lower  pipe  clay  opening •.  3 

Buff  limestone 10 

St.  Peters  sandstone , 


BEETOWN  DISTRICT. 

This  is  the  most  westerly  district  in  which  any  productive  mines  have  been  worked. 
In  former  years  they  were  very  productive,  but  have  gradually  become  less  so.  There 
are  several  subdistricts,  of  which  the  principal  ones  are  Beetown,  Nip-and-Tuck,  Mus- 
calunge,  and  Hacketts.  The  diggings  in  the  immediate  vicinity  of  Beetown  are  situated 
north  and  east  of  the  village,  chiefly  on  Sees.  20  and  29  of  T.  4,  R.  4  W.  There  are 
here  on  the  ridge  about  a  dozen  principal  old  ranges,  all  nearly  parallel,  and  bearing  a 
few  degrees  north  of  west.  They  vary  from  half  a  mile  to  a  mile  and  a  half  in  length, 
some  of  them  extending  easterly  to  the  Grant  diggings.  There  are  no  large  organized 


696  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

companies  at  work  on  them,  the  principal  product  being  by  individual  parties  in  small 
lots.  Lead  ore  is  usually  found  in  this  district  in  two  principal  openings,  known  as  the 
12- foot  opening  and  the  65-foot  opening.  The  first  is  named  from  the  height  of  the 
opening  which  usually  averages  about  12  feet.  The  second  derives  its  name  from  65 
feet  of  unproductive  rock  which  separate  it  from  the  first. 

The  following  parties  are  now  or  have  recently  been  mining  near  Beetown : 

Brown  Bros.  &  Birch.  These  diggings  are  situated  in  the  Hull  Hollow,  about 
three-quarters  of  a  mile  south  of  the  village.  They  were  discovered  in  1860  by  Walters 
&  Roberts,  and  were  first  worked  in  the  twelve  foot  opening. 

There  are  three  parallel  east  and  west  ranges  situated  about  nine  feet  apart.  They 
produce  lead  ore  which  is  found  in  flat  openings  4J£  feet  high  and  4%  feet  wide,  lying 
about  7  feet  above  the  65-foot  opening.  The  ore  has  been  traced  by  a  level  300  feet 
.  west  from  the  discovery  shaft.  The  depth  at  the  working  shaft  is  60  feet;  the  greatest 
depth  on  the  ridge  will  be  160  feet.  Work  was  commenced  in  the  winter  of  1875-G, 
since  which  time  the  product  has  been  35,000  pounds.  The  prospects  are  considered 
good. 

Wilcox  Diggings.  N.  hf.  of  S.  E.  qr.  of  Sec.  32,  T.  4.  R.  4,  W.  This  ground  has 
been  recently  bought  by  Messrs.  Henry,  Ross,  Gundry  &  Toay,  of  Mineral  Point,  by 
whom  it  is  now  operated  under  the  name  of  the  Beetown  Mine. 

Work  was  commenced  here  by  Mr.  Wilcox  in  1868.  A  level  has  been  ran  in  the 
ground  500  feet,  underlying  a  flat  sheet  of  blende  and  Smithsonite,  which  is  in  places  36 
inches  thick.  The  sheet  has  been  found  to  extend  80  feet  north  and  south,  and  130  feet 
east  and  west;  its  extreme  limits  are  not  yet  known.  On  its  south  side,  some  copper 
ore  has  been  found.  The  sheet  lies  in  the  upper  pipe  clay  opening. 

About  22  feet  above  the  sheet  of  zinc  ores  is  one  of  Smithsonite  and  lead  ore,  150  feet 
wide,  whose  length  is  unknown.  It  lies  in  flat  and  pitching  sheets  in  the  greenrock 
opening. 

The  ground  has  produced  lead  ore  to  the  value  of  $3,500;  also,  45  tons  of  Smithsonite 
and  175  tons  of  blende.  Four  men  are  now  employed  here,  and  it  is  intended  to  work 
the  mine  to  its  full  extent.  Fig.  12  shows  the  position  of  the  present  workings. 

FIG.  12. 
"-^l  \ 

^%c£.\ 
^_    \ 


rks  en  the. 

^ijjjrV/>f>erpi]pe~c7ay0feniii 

-/&?:/£:::::...? 


.^S^^^^g^^g^gs^j^^V 

Works  in  Me         \  % 


„     trorKTinlfo \^ff% 

6reenroch.Oftn.ina          XJsNSSS? 

^^^^^^^^^gswJJ 


PLAN  OF  WORKINGS  IN  THE  BEETOWN  MINE. 

Some  mining  has  also  been  done  during  this  year  (1876)  on  Sec.  27,  on  the  east  side 
of  Grant  river.  The  parties  are  as  follows: 

Josiah  Crossly  &  Co.  Produced  about  8,000  pounds  of  lead  ore  in  the  operations  of 
one  month. 

Crossly  &  Bass.  Situated  south  of  the  preceding.  Work  was  carried  on  for  six 
months,  and  stopped  by  the  owner  of  the  land;  20,000  pounds  of  lead  ore  were  produced. 

Wilcox  &  Sons.  These  parties  have  been  working  about  a  month  on  a  new  east  and 
west  range.  The  prospect  is  considered  good. 


MINES  —  BEETOWN  DISTRICT.  697 

Pigeon  Diggings. 

They  are  situated. on  the  north  half  of  Sec.  20,  T.  4,  R.  8  W.,  and  consist  of  severed 
east  and  west  ranges,  in  which  the  ore  is  found  in  flat  openings  in  the  "  Brown-rock  " 
division  of  the  Galena  limestone.  The  ground  is  owned  by  Messrs.  Barber,  Dewey  & 
Cox.  There  are  about  50  men  employed  here,  mining  chiefly  in  the  old  workings,  at  a 
depth  of  80  to  50  feet  below  the  surface.  The  annual  product  of  the  Pigeon  diggings  is 
about  250,000  pounds  of  lead  ore.  Mining  is  chiefly  confined  to  the  winter  season. 

During  the  last  year  a  sheet  of  Smithsonite  was  discovered  on  the  S.  E.  qr.  of  Sec.  19, 
which  has  produced  60  tons. 

Hacketts  Diggings. 

These  mines  are  situated  on  Sec.  17,  T.  4,  R.  4  W.  They  have  been  idle  for  several 
years.  Work  has  recently  been  resumed  on  them  by  the  following  parties:  Hutch- 
croft  &  Pigg,  and  Whitehead  &  Co.  They  have  now  good  paying  mines  in  the  65-foot 
opening.  The  annual  product  is  about  80,000  pounds. 

Nip  and  Tuck  Diggings. 

Situated  on  the  south  half  of  Sec.  25,  T.  4,  R.  5  W.  They  consist  of  several  east  and 
west  ranges,  crossed  by  north  and  south  ranges.  Very  little  mining  is  now  done  here. 
The  parties  are  Sillick  &  Co.  and  Roberts  &  Co.  The  annual  product  is  about  20,000 

pounds. 

Mnscalunge  Diggings. 

Situated  on  Sec.  26,  T.  4,  R.  5  W.  There  are  here  numerous  east  and  west  ranges, 
from  a  quarter  to  a  half  a  mile  in  length,  lying  near  Rattlesnake  creek.  More  activity 
is  displayed  here  in  mining  operations  than  anywhere  else  in  the  district,  about  half  of 
the  ore  smelted  in  the  Beetown  furnace  being  obtained  here.  In  addition  to  the  east 
and  west  ranges  already  mentioned,  there  are  a  great  number  of  small  parallel  crevices 
running  nearly  east  and  west,  and  crossed  by  various  quartering  ones,  forming  a  perfect 
net-work  of  veins  and  crevices.  The  following  parties  are  operating  in  this  vicinity : 

Graham  Mining  Company.  This  is  a  Milwaukee  company  who  own  and  work  a 
large  tract  of  ground  comprising  the  west  half  of  Sec.  26.  The  workings  are  all  in  the 
65-foot  opening.  The  following  section  of  the  Dewcy  and  Maiden  shaft  is  given,  which 

shows  the  position  of  strata  from  the  top  of  the  ridge  downward : 

feet. 

Soil  and  clay 15 

Galena  limestone 38 

Tough,  light  rock,  hard  and  flinty 2 

Opening  from  5  to  12  feet  high 12 

Hard  rock  with  layers  of  flint 65 

Opening  (workings) 13 

Galena  limestone  to  top  of  Trejiton 35 

Total  thickness 180 

The  two  openings  are  seen  here  to  be  separated  by  65  feet  of  intervening  barren  rock. 
The  ground  is  drained  by  a  level,  about  three-quarters  of  a  mile  long,  run  on  the  ran- 
dom of  the  lower  opening,  at  an  expense  of  $20,000.  It  empties  into  one  of  the  adja- 
cent branches  of  Rattlesnake  creek.  It  could  easily  be  drained  to  the  top  of  the  Blue 
limestone,  by  a  level  in  the  horizon  of  the  Pipe-clay  opening. 

A  convenience  in  hoisting  was  noticed  here  which  might  profitably  be  adopted  in  other 
portions  of  the  Lead  region.  A  six-inch  hole  had  been  drilled  from  the  surface  to  one 
of  the  drifts  for  purposes  of  ventilation.  An  Artesian  well  bucket  was  then  put  on,  and 
all  small  stuff  and  wash-dirt  was  removed  through  the  hole,  thus  saving  a  long  and  un- 


698 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


FIG. 13. 


necessary  transportation  underground  to  the  main  shaft.  The  company  has  worked 
continuously  here  for  many  years,  and  now  employs  about  fifteen  men.  The  ground  has 
been  very  productive;  it  produced  in  one  year  1,300,000  pounds.  Its  average  annual  pro- 
duction for  the  last  nine  years  is  estimated  at  300,000  pounds  of  lead  ore. 

James  Thomas  &  Co.  This  company  has  been  working  here  for  the  last  fifteen  years. 
The  ore  is  found  on  an  east  and  west  range,  in  the  65-foot  opening.  The  diggings  arc 
dry  and  from  150  to  160  feet  deep.  Four  men  are  employed  here.  The  average  pro- 
duct is  150,000  pounds  of  lead  ore  per  annum.  The  land  is  owned  by  Mr.  Dewey. 

Hntchcroft  &  Thomas.  Situated  450  feet  south  of  the  preceding,  and  connected 
with  them  underground.  They  are  in  the  same  opening  as  the  preceding,  and  have 
been  worked  continuously  many  years.  During  the  last  year  they  have  been  idle,  hav- 
ing been  sold  by  the  parties  who  operated  them.  When  worked,  then:  annual  product 
was  150,000  pounds. 

Hiitchinson,  Dewey  &  Co.  Situated  on  the  S.  E.  qr.  of  Sec.  26,  east  of  James  Thom- 
as &  Co.,  and  on  the  same  range  and  opening.  This  party  has  been  working  here  since 
1869,  and  has  now  a  very  good  prospect.  The  average  depth  below  the  surface  is  160 

feet;  in  some  cases  it  is  180  feet.  They  are 
connected  with  the  Adkinson  diggings  by  a 
quartering  range.  They  have  produced  about 
30,000  pounds  in  the  last  three  years.  Three 
men  are  now  employed. 

Adkinson  Diggings.  Situated  a  short  dis- 
tance east  of  the  preceding  and  connected 
with  them.  Access  is  gained  to  these  diggings 
through  a  level  about  a  quarter  of  a  mile  long, 
emptying  into  the  valley  of  Rattlesnake  creek. 
The  level  was  run  on  a  northeast  crevice, 
which  contained  a  large  amount  of  ore,  and 
was  frequently  intersected  with  east  and  west 
crevices,  as  represented  in  Fig.  13.  These  dig- 
JUNCTION  OF  EAST  AND  WEST  VEINS  -WITH  A  —„„,  navf>  hppn  worked  continuously  durine- 
QUARTERING  RANGE,  ADKINSON  DIGGINGS.  S1"^8  J 

.    the  last  twenty  veal's.     During  the  last  fifteen 
1.  Northeast  or  quartering  range;  2,  3,  4.  East 

and  west  veins.  „     years  the  annual  product  has  been  150,000 

pounds  of  lead  ore.    Four  men  are  now  employed  here. 

Showalter  &  Payten.  Situated  a  quarter  of  a  mile  sDutheast  of  the  preceding,  and 
near  the  south  line  of  the  Dewey  land.  These  parties  commenced  two  years  since,  and 
are  now  working  an  east  and  west  range  in  the  65-foot  opening.  Two  men  are  now 
working  here,  and  the  prospect  is  good.  During  the  last  two  years  the  product  has  been 
70,000  pounds. 

Arthur  &  Co.  Situated  200  feet  south  of  the  preceding,  on  Mr.  Arthur's  land.  This 
is  a  new  east  and  west  range,  discovered  in  the  spring  of  1876.  A  shaft  has  been  sunk 
90  feet  to  the  65-foot  opening,  and  a  small  amount  of  ore  produced.  The  appearances 
in  this  new  range  arc  quite  encouraging. 

Hitter  &  Bock.  N.  E.  qr.  Sec.  35,  T.  4,  R.  5  W.  Situated  on  land  owned  by  Mr. 
Ritter.  fhis  is  a  new  east  and  west  range,  discovered  in  the  summer  of  1875.  It  is 
worked  on  the  65-foot  level.  It  is  regarded  as  a  good  prospect,  and  has  already  pro- 
duced 20,000  pounds. 

Loomis  &  Co.  Situated  on  the  land  of  the  Graham  Mining  Co.,  in  the  southern 
part.  This  is  also  a  new  east  and  west  range,  discovered  in  August,  1876.  It  has  pro- 
duced about  12,000  pounds.  The  mine  is  now  in  a  condition  to  yield  1,000  pounds  per 
day. 

The  Lead  ore  in  the  Muscalunge  mines  occurs  in  direct  contact  with  the  wall  rock, 


MINES  — POTOSI  DISTRICT. 


699 


usually  in  vertical  sheets,  and  without  any  of  the  associate  vein-minerals  which  are  usu- 
ally found  in  the  other  mining  districts. 


FIG.  14. 


POTOSI  DISTRICT. 

Mining  operations  here  are  chiefly  confined  to  the  winter  season,  and  furnish  employ- 
ment to  about  twenty  miners. 

The  old  ranges  of  the  Potosi  diggings  «re  included  in  Sees.  33  and  34,  T.  3,  R.  3  W. 
Their  general  course  is  about  N.  70°  W.,  although  some  bear  a  few  degrees  more  to 
the  west,  and  some  a  few  more  to  the  north.  They  numbered  about  thirty  in  all,  which 
were  considered  as  separate  and  distinct  ranges ;  and  in  addition  there  were  many 
smaller  crevices  not  sufficiently  important  to  constitute  ranges  by  themselves. 

Among  the  more  important  were  the  Long,  Wooley,  Gillet,  Gilmore,  Smith,  Polking- 
horn  and  Barbara,  some  of  which  were  over  a  mile  in  length. 

The  productive  portion  of  these  ranges  is  confined  to  the  middle  and  lower  portions  of 
t!  ie  Galena  limestone,  none  of  the  crevices  having  as  yet  been  proved  as  low  as  the 
Brown  rock;  the  ore  is  usually  found  in  sheets  of  varying  thickness. 

Considerable  irregularity  exists  in  the  form- 
ation of  many  of  the  crevices  in  the  Potosi 
district,  by  which,  they  seem  to  split  up 
in  the  lower  beds  of  the  limestone,  forming 
key- rocks  and  divergent  crevices.  An  instance 
in  point  was  seen  in  the  diggings  of  Mr. 
Meredith,  in  the  N.  E.  qr.  of  Sec.  33,  about 
300  feet  south  of  the  old  Wooley  range,  on 
the  summit  of  the  ridge. 

A  shaft  was  sunk  on  the  main  crevice  which 
continued  without  change  for  sixty  feet  from 
the  surface.  At  this  point  a  hard  key-rock, 
as  it  is  called,  was  encountered,  on  which 
the  crevice  and  ore  sheets  divided,  one  part 
continuing  vertical,  and  the  other  slanting 
downward  at  an  angle  of  about  45°  for  a 


distance  of  thirty  feet.  Here  a  vary  hard  and 
smooth  floor  was  found  on  which  the  sheet 
was  followed  out  by  drifting,  for  a  distance  of 
one  hundred  and  thirty  feet  without  reaching 
the  end.  No  appearance  of  openings  was 
observed.  These  diggings  were  struck  about 
six  years  ago  (1870)  and  have  produced  since 
then  about  420,000  Ibs. 


SECTION  OF  THE  MHRBDITH  MINE. 


Rockville  Diggings. 

There  are  here  a  number  of  east  and  west  ranges  with  flat  openings,  which  have  been 
worked  with  but  little  interruption  since  1840,  and  now  furnish  employment  to  about 
twenty  miners.  Mining  is  chiefly  confined  to  the  winter  season.  The  following  parties 
are  now  operating  here. 

Phillips  &  Walker.  S.  W.  qr.  of  S.  W.  qr.,  Sec.  13,  T..3,  R.  3W.  These  parties 
are  working  a  new  east  and  west  range,  discovered  by  them  in  the  summer  of  1874. 
The  ore  is  found  at  a  depth  of  about  100  feet  below  the  surface,  in  flat  openings  from  50 
to  60  feet  wide,  whose  length  has  not  yet  been  ascertained.  They  have,  however,  been 
worked  to  a  distance  of  300  feet.  The  lead  ore  is  found  in  what  is  known  here  as  the 


700  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

second  opening,  which  lies  about  30  feet  above  the  upper  surface  of  the  Blue  limestone. 
Their  annual  production  is  30,000  Ibs. 

Dilger  Mine.  N.  W.  qr.  of  N.  W.  qr.  Sec.  24.  This  is  a  new  range  discovered  in 
January,  1876.  The  works  are  as  yet  confined  to  the  first  opening,  which  is  here  30  feet 
above  the  second.  It  has  produced  during  the  past  year  40,000  pounds. 

Hayward  Range.  6.  W.  qr.  Sec.  13.  This  range  has  been  worked  continuously 
every  winter  since  its  discovery  in  1841,  and  has  yielded  in  all  between  four  and  five 
million  pounds.  It  is  now  worked  by  Messrs.  Jackson  &  Galloway  in  the  second  open- 
ing, which  is  here  from  30  to  40  feet  wide.  It  produces  about  100,000  pounds  per  an- 
num. 

Warfield  Range.  S.  W.  qr.  Sec.  13.  This  range  has  been  worked  every  winter 
during  the  last  thirty  years,  and  has  produced  about  2,000,000  pounds.  It  is  now 
worked  by  Messrs.  White  &  Dunn  in  the  second  opening,  which  is  here  from  30  to  40 
feet  wide.  Its  annual  product  is  about  100,000  pounds. 

Cuniow  and  Pillow  Range.  S.  W.  qr.  Sec.  13.  This  range  has  not  been  idle 
during  the  last  thirty  years,  and  is  still  productive.  During  the  last  fifteen  years  the 
range  has  produced  over  100,000  pounds  per  annum.  Messrs.  Nichols  &  Stephens  are 
now  mining  on  it,  and  producing  20,000  pounds  per  annum. 

Emery  and  Davis  Level.  N.  W.  qr.  of  N.  W.  qr.  Sec.  24.  The  level  was  com- 
menced in  1852,  and  is  now  600  feet  long,  and  drains  the  ground  in  its  vicinity  nearly 
as  low  as  the  second  opening;  its  cost  was  about  $20,000.  The  excavations  here  were 
of  the  nature  of  a  quarry,  several  flat  sheets  of  lead  ore  being  found  interstratified  with 
the  Galena  limestone.  While  the  level  was  in  operation,  the  annual  product  was  about 
100,000  pounds.  The  level  drains  the  Langstaff  and  Willey  ranges,  which  were  discov- 
ered about  thirty  years  ago,  and  have  been  worked  continuously  ever  since.  Most  of 
the  lead  ore  is  obtained  from  the  first  opaning ;  the  annual  product  is  50,000  pounds. 
These  ranges  have  been  worked  to  the  present  water  level,  leaving  sheets  of  ore  from 
12  to  18  inches  thick  going  down.  The  level  should  be  run  a  few  rods  farther  to  con- 
nect with  a  noith  and  south  crevice;  it  would  then  probably  drain  all  the  ranges  much 
deeper. 

Stone  &  Bryhon.  Situated  near  the  N.  W.  corner  of  Sec.  1,  T.  3,  R.  3  W.,  on 
land  owned  by  Mr.  Stone,  about  three  miles  north  of  the  village  of  Rockville.  The 
works  are  in  the  first  opening,  which  is  from  eight  to  ten  feet  wide.  They  have  been 
worked  in  the  winter  season  during  the  last  four  years,  producing  annually  between 
30,000  and  40,000  pounds.  They  were  formerly  worked  by  Mr.  Grusham  and  were 
more  productive.  The  mines  are  dry. 

Griswold  Diggings.  Situated  about  a  quarter  of  a  mile  south  of  the  preceding. 
These  are  dry  diggings  worked  in  the  first  opening,  which  is  here  about  six  feet  high 
and  from  ton  to  thirty  feet  wide.  They  have  been  worked  continuously  during  the  last 
seven  years,  producing  about  65,000  pounds  per  annum. 

Henry  Gillilan's  Diggings.  These  diggings  are  situated  about  three  miles  south- 
east of  Rockville,  on  the  Platte  river.  They  are  dry  diggings,  and  have  been  worked 
during  the  last  four  years,  in  the  first  opening,  which  is  here  thirty  feet  wide  and  about 
six  feet  high.  The  annual  product  is  25,000  pounds. 

British  Hollow  Diggings. 

But  little  mining  is  now  done  in  these  mines.  In  the  winter  saason  about  twenty 
men  are  employed.  The  following  parties  are  now  mining  here: 

J.  Alderson's  Diggings.  N.  W.  qr.  Sec.  26,  T.  3,  R.  3  W.  They  are  situated  on 
the  Craig  range  in  the  village  of  British  Hollow.  This  range  was  worked  by  a  Cincin- 
nati company  for  three  years;  they  abandoned  it  two  years  ago.  This,  company 
produced  about  three  million  pounds  during  the  time  of  their  operations.  Mr.  Alder- 


MINES  -  FAIRPLAY  DISTRICT.  701 

son  commenced  mining  here  again  in  July,  1876,  with  a  steam  pump,  and  has  sunk  four 
shafts.  The  workings  are  about  120  feet  deep  in  the  second  opening,  and  in  the  third, 
which  is  about  25  feet  below  the  second.  The  mine  has  not  produced  much  yet,  as  the 
time  has  been  mostly  consumed  in  preliminary  operations. 

Peak  &  Blair.  N.  W.  qr.  Sec.  26.  These  parties  have  also  been  working  on  the 
Craig  range  during  the  past  summer  (1876).  They  have  a  flat  sheet  of  lead  ore  about 
five  inches  thick  in  the  first  opening,  which  here  averages  20  feet  in  width.  This  range 
has  been  worked  during  the  last  forty  years.  The  product  of  the  present  parties  has 
been  about  20,000  pounds. 

Dutch  Hollow  Diggings. 

They  are  situated  on  the  north  half  of  Sec.  36,  T.  3,  R.  3  W.,  about  two  and  a  half 
miles  east  of  Potosi.  The  following  parties  are  now  operating  here: 

Dutch  Hollow  Level  Company.  Mining  operations  have  been  earned  on  here  con- 
tinuously for  the  last  six  years,  excavating  a  level  on  or  near  the  upper  surface  of  the 
Blue  limestone.  The  level  is  now  about  half  a  mile  long,  and  it  is  expected  to  reach  the 
main  shaft  in  about  a  month.  When  completed,  the  level  will  unwater  all  the  Galena 
limestone  above  it,  which  is  here  about  one  hundred  feet  thick.  It  is  expected  to  un- 
water the  Kendall,  and  many  other  old  ranges  in  the  vicinity,  as  deep  as  the  third  open- 
ing. The  level  is  not  producing  much  now.  During  the  year  1872,  it  produced  60,000 
pounds. 

Rnp  &  Son.  X.  E.  qr.  Sec.  35.  This  party  has  been  working  during  the  last  six 
months  on  a  part  of  the  Ziig  range.  The  ore  is  found  in  the  first  opening,  which  is 
here  about  15  feet  wide.  The  production  has  been  150,000  pounds. 

Zug  Diggings.  This  is  an  east  and  west  range,  being  the  same  range  and  opening 
as  the  preceding.  It  is  worked  to  a  depth  of  75  feet.  The  present  party  has  mined 
here  during  the  last  year  and  a  half,  and  produced  150,000  pounds. 

LangstafP  &  Gillan.  Situated  three-quarters  of  a  mile  northeast  of  the  preceding, 
on  the  creek  in  Sec.  25.  The  lead  ore  is  found  here  in  a  flat  sheet  in  the  first  opening, 
near  the  water  level  and  about  30  feet  below  the  surface.  Three  men  have  been  work- 
ing here  twelve  months,  and  have  produced  60,000  pounds. 

The  production  of  the  Potosi  district,  including  Rockville,  British  Hollow  and  Dutch 
-  Hollow,  could  not  be  definitely  ascertained,  as  very  little  record  has  been  kept  of  it.  It 
is  estimated  at  80,000  pounds  per  annum. 

Mining  in  this  district  is  generally  abandoned  in  summer  for  farming,  and  resumed 
again  in  the  winter,  in  the  lack  of  other  employment.  In  this  way  a  large  number  of 
men  are  at  work  in  the  winter,  each  raising  a  small  amount  by  prospecting,  which  forms 
in  the  aggregate  the  total  product  of  the  district. 

FAIRPLAY  DISTRICT. 

The  only  mines  in  this  vicinity  which  have  recently  produced  anything  are  those  of 
Black  &  Co.,  on  the  N.  E.  qr.  of  Sec.  24,  T.  1,  R.  2  W.,  and  those  of  Williams  &  Co., 
near  the  center  of  Sec.  19,  T.  1,  R.  1  W. 

Black  &  Co.  This  property,  which  comprises  in  all  about  two  hundred  and 
forty  acres,  is  owned  by  Messrs.  Joseph  and  Thomas  Sparks.  It  has  been  known  to  be 
rich  ground  for  many  years,  and  to  contain,  besides  the  ore,  an  immense  amount  of  water, 
which  was  the  chief  obstacle  t&  be  overcome.  Previous  to  the  operations  of  Mr.  Black, 
it  had  been  attempted  by  three  separate  parties,  at  as  many  different  times,  but  always 
with  more  or  less  loss. 

Mr.  Black  commenced  work  on  it  in  November,  1871,  by  means  of  pumping,  and 


702  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

continued  to  add  pumps,  engines,  and  pumping  machinery  at  intervals.  At  the  time 
the  mine  was  visited  (June,  1874),  there  were  in  operation  two  steam  pumps,  and  two 
large  lift,  pumps,  together  with  three  boilers  and  two  engines,  one  of  them  about  thirty 
horse  power.  The  company  then  contemplated  adding  a  larger  engine  and  machinery. 
It  was  estimated  that  about  a  thousand  gallons  of  water  per  minute  were  being  pumped 
from  the  mme,  and  when  the  lower  opening  is  reached,  which  is  thought  to  be  about 
fifteen  feet  deeper,  it  will  become  necessary  to  pump  about  fifteen  hundred  gallons  per 
minute. 

The  mine  is  in  the  upper  beds  of  the  Galena  limestone,  which  is  here  present  in  its 
full  thickness,  and  indeed  the  first  few  feet  of  the  shafts  are  sunk  through  the  lowest  bed  of 
the  Cincinnati  group,  as  may  be  seen  from  the  yellow  clay  with  the  characteristic  shells 
in  any  of  the  shallow,  prospecting  holes  in  the  vicinity.  The  following  section  of  the 
strata,  penetrated  in  sinking  the  pump-shaft,  will  give  a  correct  idea  of  the  formations 
here  represented: 

Cincinnati   Group. 

Ft.    In,, 

Soil  and  clay  bed 20 

Pipe  clay 10 

Bed  of  black  clay 4 

Shaly  layers 10 

Galena  Limestone. 

Galena  limestone  in  thin  layers 4 

Galena  limestone  cap  in  layers  4  feet  thick,  gradually  increasing  in 

thickness  to  the  bottom 30 

Opening  containing  ore 30 


Total  depth  of  shaft 86    00 


The  course  of  the  vein  is  nearly  east  and  west,  and  five  shafts  have  been  sunk  upon 
it,  the  deepest  of  which  has  reached  a  point  105  feet  below  the  surface.  The  opening 
now  presents  the  appearance  of  a  series  of  large  rooms  or  caves,  from  15  to  20  feet  wide 
and  about  15  feet  high,  for  a  distance  of  600  feet. 

The  vein  was  crossed  in  several  places  by  bars  of  hard  rock,  one  of  which  was  sixty- 
five  feet  in  thickness.  The  bars  always  caused  a  decrease  in  the  size  of  the  opening, 
and  sometimes  nearly  cut  off  the  vein.  In  other  places  the  opening  contracted  in  width, 
in,  wMch  case  the  ore  usually  occurred  in  a  solid  sheet,  sometimes  as  much  as  seven  feet 
tluck  by  seven  and  a  half  high.  In  the  caves  or  larger  parts  of  the  opening  the  ore  was 
found  in  large  masses,  weighing  sometimes  several  thousand  pounds.  Two  large  mas- 
ses were  found  which  weighed  respectively  fifty  thousand  and  twenty-seven  thousand 
pounds.  With  the  ore  large  masses  of  rock  were  found  mixed  with  loose  dirt  and  a  fine 
dark  clay.  The  sides  of  the  opening  were  much  washed  and  worn  by  water,  showing 
a  very  regular  stratification  with  no  appearance  whatever  of  faults  or  dislocations.  Each 
of  the  caves  in  the  opening  had  a  chimney  going  down,  apparently  to  a  second  open- 
ing, which  has  never  yet  been  proved  or  worked.  The  upper  part  of  the  opening  was 
sometimes  filled  with  a  large  key-rock,  having  a  crevice  on  each  side  of  it.  Some- 
times, however,  the  key-rock  was  replaced  by  a  flat-cap-rock  containing  crevices. 

The  appearance  of  these  caverns  as  we  passed  through  them  was  a  sight  not  soon  to 
be  forgotten.  On  the  floor  lay  great  masses  of  rock  which  had  fallen  from  a  bove,  with 
clay  continually  moistened  from  the  dripping  walls  and  arching  roof,  and  here  and  there 
the  feeble  light  revealed  rich  masses  of  glittering  ore. 


MINES  — FAIRPLAY  DISTRICT. 


703 


FIG.  15. 


The  annexed  section  shows  the  relative  position  of  the  differ- 
ent portions  of  the  vein : 
.     1.  Crevice  containing  lead  ore. 

2.  Key-rock  with  crevices  on  each  side. 

3.  Opening  containing  lead  ore  with  loose  masses  of  rock  and 
clay. 

4.  Chimney  going  down  to 

5.  Second  opening. 

6.  Galena  limestone. 

The  vein  has  not  been  worked  over  half  the  time  since  its 
commencement,  as  frequent  stoppages  were  necessary  for  the 
purpose  of  putting  in  new  pumps  and  machinery.  Work  was 
discontinued  here  in  February,  1876,  but  it  is  expected  that  act- 
ive operations  will  soon  be  resumed. 

Mr.  Black  estimated  that  he  had  taken  out  about  one  million 
pounds  of  lead  ore,  at  an  expense  of  $40,000. 

Williams  &  Co.  This  mining  property  is  situated  about 
three-quarters  of  a  mile  northeast  of  Black's  mine,  and  was  op- 
erated by  the  proprietors,  Messrs.  Thomas,  and  Jeremiah  Wil- 
liams, and  Mr.  O'Connor.  The  water  in  this  ground  is  not 
nearly  so  abundant  as  in  the  preceding.  It  is  easily  removed 
with  a  common  lift-pump,  worked  with  a  ten-horse  power  en- 
gine; the  amount  seldom  exceeds  250  gallons  per  minute.  Mining  has  been  confined 

to  the  upper  half  of  the  Galena  limestone.    The  lower  clay  beds  of  the  Cincinnati  group 

are  also  found  here,  but  there  is  not  so  great  a  thickness  of  them  as  at  Black's  mine. 

The  pump  shaft  commences  at  the  top  of  the  Galena  limestone,  and  is  sunk  to  a  depth 

of  one  hundred  and  six  feet,  at  which  point  the 

top  of  the  second  opening  is  found,  after  passing 

through  the  first  opening,  which  is  situated  at  a 

depth  of  forty-seven  feet  from  the  surface,  and  is 

probably    identical    with    the    first    opening   at 

Black's  mine,  which  it  much  resembles  in  its  gen- 
eral appearance.    The  first  opening  here  consists 

of  a  series  of  large  caves  or  enlargements  of  the 

crevice,  with  chimneys  going  down  to  the  second 

opening. 
The  ore  was  found  in  masses  mixed  with  clay  and 

large  pieces  of  stone  which  had  apparently  fallen 

from  the  roof  or  cap.    The  Lead  ore  from  its  great- 
er specific  gravity  usually  occupies  the  lower  part 

or  floor  of  the  opening.    The  course  of  the  range 

is  very  nearly  east  and  west,  but  bears  a  little 

north  on  its  western  end.    The  length  of  drifts  in 

the  top  opening  amounts  to  about  nine  hundred 

feet.     It  is  about  worked  out  at  the  western  end, 

but  still  continues  good  at  the  east.      Several 

masses  of  lead  ore  were  found  in  this  opening 

weighing  from  fourteen  to  fifteen  thousand  pounds. 

A  singular  formation  of  ore  was  found  in  the  top    SECTION  OF  OPENING  IN  THE  WILLIAMS 

opening,  as  illustrated  in  the  annexed  diagram. 

1.  Opening  and  crevice  filled  with  loose  masses  of  lead  ore  and  rock,  mixed  with  loose 

fine  clay  and  sediment.    2.  This  is  a  bench  about  a  foot  in  width  on  each  side  of  the  opeu- 


704:     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

ing,  and  extending  along  the  entire  length  of  the  cave,  a  distance  of  80  feet,  on  which 
shelf,  and  the  sides  immediately  above  and  adjacent,  the  ore  was  deposited,  fastened 
firmly  to  the  wall,  and  exposing  crystalline  faces  to  the  center  of  the  opening.  In  other 
portions  of  the  mine  this  bench  was  not  observed,  and  the  ore  was  usually  attached  in 
sheets  to  the  side  of  the  opening.  3.  The  lower  opening.  4.  The  Galena  limestone. 

The  mine  was  discovered  and  opened  in  February,  1872,  and  since  then  has  proba- 
bly been  the  most  productive  and  remunerative  mine  in  the  district,  on  account  of  the 
comparatively  small  amount  of  water  to  contend  with,  and  the  large  amount  of  lead 
ores  obtained,  which  has  been  estimated  at  two  and  a  half  million  pounds.  Work  was 
suspended  on  this  mine  in  the  fall  of  1875,  and  lias  not  since  been  resumed. 

Fairplay  Level  Co.  A  company,  consisting  of  Messrs.  Merry,  Olinger,  Rewell, 
Pier  and  Notte,  having  formed  a  stock  company  with  a  capital  of  $50,000,  have  been 
engaged  during  the  last  eight  years  in  running  a  level  on  land  owned  by  George 
Siddell  &  Co.  The  level  is  commenced  on  the  E.  half  of  the  S.  W.  qr.  of  Sec.  26,  T.  1, 
R.  2  W..,  about  three-quarters  of  a  mile  below  the  village  of  Fairplay.  It  has  been  run 
eastward  a  distance  of  2,200  feet,  and  thence  south  70  feet;  and  has  cost  about  $30,000. 
One  "shift"  of  three  men  is  the  usual  number  employed,  and  it  is  not  expected  that 
the  level  will  be  completed  for  many  years.  Its  greatest  depth  below  the  surface  is  140 
feet,  and  48  feet  below  the  natural  water  level;  one  mile  farther  east  it  will  drain  about 
60  feet  below  the  present  water  level. 

This  level  will  unwater  the  whole  of  section  25,  and  will  cut  the  following  ranges  in 
the  tln'rd  opening:  The  Crabtrets,  Thompson,  Engine,  Cams,  Bruce,  Lost  range, 
Franklin,  Seward,  and  Cave  range.  The  openings  in  these  ranges  are  vertical;  they 
were  formerly  worked  and  abandoned  with  lead  ore  in  them  going  below  the  water. 
When  these  ranges  are  unwatered  they  will  undoubtedly  be  very  productive. 

In  the  vicinity  of  Fairplay,  about  fifty  men  find  employment  in  mining  during  the 
winter;  in  summer  the  mines  are  idle.  The  greater  part  of  the  lead  ore  raised  in  this 
district  comes  from  the  mines  south  of  the  village,  and,  exclusive  of  the  two  large  mines 
previously  described,  has  not  exceeded  50,000  pounds  per  annum  for  the  last  six  years. 

HAZEL  GREEN  DISTRICT. 

The  Hazel  Green  district  exhibits  considerable  activity  at  present  in  mining  opera- 
tions; and  the  reports  of  smelters  in  this  vicinity  show  that  a  large  amount  of  ore  is 
raised  here.  During  the  years  1872  and  1873,  miners  were  attracted  to  other  localities 
by  the  prospect  of  higher  wages,  which  caused  a  temporary  decrease  in  the  production 
of  lead  ore;  the  mines,  however,  remained  unimpaired.  The  miners  have  now  returned, 
and  the  mines  have  regained  their  normal  productive  condition. 

The  most  remunerative  and  continuously  productive  portion  of  the  district  is  the  prop- 
erty of  the  Hazel  Green  Mining  Company,  otherwise  known  as  Crawford,  Mills  &  Co. 
It  is  situated  on  the  N.  W.  qr.  of  Sec.  30,  part  of  the  S.  W.  qr.  of  Sec.  30,  part  of  the  N. 
E.  qr.  of  Sec.  30,  part  of  the  S.  E.  qr.  of  Sec.  19,  the  S.  W.  qr.  of  Sec.  19,  the  N.  W.  qr. 
of  Sec.  19,  the  W.  hf.  of  the  S.  W.  qr.  of  Sec.  18,  all  in  T.  1,  R.  1  E.;  also  the  N.  E. 
qr.  of  Sec.  24,  and  the  E.  hf.  of  the  E.  hf.  of  Sec.  25,  T.  1,  R.  1,  W.,  comprising  in  all 
eleven  hundred  and  six  acres,  on  which  over  four  hundred  and  fifty  distinct  mineral 
veins  have  been  discovered  and  worked. 

During  the  early  days  of  mining  these  grounds  were  wo  'ked  from  the  surface  as  deep 
as  was  then  possible,  which  was  only  about  thirty-five  feet,  when  they  had  to  be  aban- 
doned. Pumping  was  tried  on  some  of  the  larger  bodies  of  ore,  but  as  a  general  thing 
was  found  to  be  too  expensive  to  be  very  remunerative,  on  account  of  the  vast  amount 
of  water  which  the  ground  contained.  In  the  year  1862,  Crawford,  Mills  &.Co.  com- 
menced their  level  from  a  point  on  the  Hard  Scrabble  Branch,  and  have  been  working 


MINES  —  HAZEL  GREEN  DISTRICT.  705 

it  continuously  ever  since.    Its  total  completed  length  is  now  about  four  thousand  feet. 

It  is  a  feature  of  this  ground  that  it  is  traversed  by  several  bars  or  belts  of  ground 
which  are  very  hard  and  impervious  to  water.  As  soon  as  the  level  is  driven  through 
one  of  them,  it  unwaters  the  ground  in  all  directions  to  the  next  bar. 

Sometime  in  the  year  1871,  one  of  those  bars  was  reached  which  was  so  hard  that  blast- 
ing with  powder  made  but  little  impression  on  it.  As  an  experiment,  nitro-glycerme 
was  tried  and  gave  the  greatest  satisfaction,  so  much  indeed  that  a  factory  has  been  es- 
tablished here,  and  it  is  gradually  being  introduced  into  the  mines.  It  is  at  present 
used  in  Dubuque,  Galena,  New  Diggings  and  several  other  places.  It  was  at  first  re- 
garded with  some  dislike  and  distrust  by  the  miners,  but  this  prejudice  is  fast  being 
overcome,  and  nitro-glycerine  or  some  of  its  compounds  will  probably  supplant  gun- 
powder in  the  mines  at  no  distant  day.  The  factory  at  Hazel  Green  produced,  during 
the  first  three  years,  about  three  thousand  pounds  of  nitro-glycerine,  and  the  demand  is 
steadily  increasing. 

On  account  of  the  position  of  the  bars,  it  was  found  necessary  to  make  three  branches 
to  the  level,  one  of  which  is  now  completed  and  is  gradually  draining  the  western  part 
of  the  ground.  The  northern  branch  when  completed  will  undoubtedly  unwater.the 
rest  of  the  ground. 

This  level  is  an  evidence  of  what  can  be  done  by  scientific  mining,  when  carried  on 
persistently  and  systematically,  with  sufficient  capital,  applied  with  foresight  and  saga- 
city. It  has  cost  the  company  twelve  years  of  time  and  about  $100,000.  Its  results  are, 
that  it  has  already  repaid  the  outlay  of  capital  by  the  ore  raised  from  the  ground  un- 
watered  by  it,  which  would  otherwise  have  been  inaccessible.  When  completed,  it  will 
unwater  the  ground  135  feet  below  the  natural  water  level  on  the  ridge  It  furnishes 
employment  to  about  80  miners  during  the  mining  season,  which  without  it,  would 
hardly  exceed  half  a  dozen. 

Quite  a  large  and  clear  stream  of  water  is  discharged  from  the  niouth  of  the  level, 
and  is  at  present  used  to  operate  a  furnace  and  three  wash-places. 

The  ore  in  the  Hazel  Green  mines  is  usually  found  in  sheets;  this  is  its  charac- 
teristic mode  of  occurrence.  The  ranges  are  approximately  east  and  west,  or  north 
and  south,  the  former  being  the  most  productive.  Ore  is  also  sometimes  found  in  large 
bunches  or  pockets,  containing  sometimes  several  thousand  pounds,  and  occasionally  in 
openings.  The  pockets  are  often  Lined  with  large  and  very  regular  cubes,  affording 
handsome  cabinet  specimens.  The  total  production  since  the  discovery  of  these  mines 
has  been  carefully  computed  from  the  smelter's  accounts  at  about  126,000,000  pounds. 
Their  present  product  is  about  800,000  pounds  per  annum. 

Mining  in  this  vicinity  is  confined  to  the  upper  half  of  the  Galena  limestone,  which  is 
here  present  in  its  entire  thickness,  the  clay  of  the  lower  beds  of  the  Cincinnati  group 
being  found  near  the  village,  on  the  road  to  Galena.  A  section  of  the  strata  from  the 
top  of  the  ridge  to  the  level  would  present  approximately  the  following  features: 

Soil  and  flints 15  feet. 

Galena  limestone 90    " 

Shales  or  thin  layers  of  limestone 10    " 

First  clay  opening 10     " 

Second  clay  opening 20    " 

Flint  opening  to  floor  of  level 20    " 

Total  thickness 165    " 

The  following  are  the  parties  who  are  now  engaged  in  mining  on  the  company's  land 
or  have  been  during  the  course  of  the  present  survey: 
Wis.  SUR.— 45 


706     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

Richard  Eustice  &  Co.  These  parties  were  working  in  a  new  locality,  and  had,  at 
the  time  they  were  visited,  one  of  the  handsomest  displays  of  ore  ever  seen  in  the 
grounds.  The  bottom  of  the  shaft  had  penetrated  an  opening  filled  with  soft  earth. 
The  sides  of  the  opening  were  lined  with  a  body  of  ore  which  presented  an  unbroken 
mass  of  cubic  crystals  of  various  sizes,  some  of  them  being  as  much  as  six  inches  on  a 
side,  and  of  very  perfect  shape,  affording  very  handsome  cabinet  specimens.  There 
was  not  less  than  10,000  pounds  of  lead  ore  in  sight,  in  a  place  about  ten  feet  long. 
This  body  of  ore  is  known  to  continue  several  feet  deeper  to  the  drift  below.  These 
diggings  were  worked  until  the  fall  of  1875,  and  produced  in  all  120,000  pounds. 

Rowe  &  Rowe.  This  is  a  new  range,  and  was  discovered  in  March,  1874.  It  is  an 
east  and  west  sheet,  in  which  the  ore  occurs  in  a  crevice  three  or  four  inches  wide,  at  a 
depth  of  about  60  feet  below  the  surface,  and  about  35  feet  above  the  flint  opening. 
Work  was  suspended  here  in  September,  1876.  The  total  amount  produced  to  that 
time  was  50,000  pounds. 

Richard  Eustice'  Diggings.  Situated  on  the  Phelps  r,ange,  shafts  are  90  feet  deep, 
down  to  the  clay  openings.  Length  of  drifts  about  150  feet.  The  ore  here  occurs  in  a 
sheet  about  an  inch  thick.  The  diggings  were  worked  from  June,  1872,  to  June,  1875, 
and  produced  about  40,000  pounds.  Near  these  diggings,  and  about  ten  feet  deeper,  is 
an  east  and  west  sheet  dipping  to  the  north,  carrying  bunches  of  blende,  which  affords 
quite  handsome  crystals. 

Manwaring  and  Madison  Range.  This  is  an  east  and  west  range,  and  is  some- 
times known  as  the  Hinch  range,  from  the  name  of  a  party  who  formerly  worked  it,  and 
by  whom  it  was  abandoned  in  1858.  Since  the  level  has  been  run,  the  water  has  fallen 
about  50  feet  in  this  ground,  and  in  December,  1873,  work  was  resumed  on  it  by  Craw- 
ford, Mills  &  Co.,  since  which  time  it  has  produced  40,000  pounds  of  lead  ore.  The 
shaft  is  down  about  fifty-five  feet,  or  within  six  feet  of  the  flint  opening.  Work  was 
suspended  on  it  in  June,  1875. 

John  Edwards'  Diggings.  Situated  a  short  distance  further  west  on  the  same 
range.  A  flat  sheet  of  blende  is  found  here  in  the  second  opening,  at  a  depth  of  80  feet 
below  the  surface.  The  order  of  deposition  here  is :  1st,  pyrite;  2d,  galemte;  3d,  blende. 
During  the  winter  of  1875-6,  the  product  was  blende,  10  tons;  lead  ore,  1,400  pounds. 

Bull  Pump  Range.  This  range  was  worked  by  Jackson  &  Co.  during  the  years 
1873-4-5,  producing  90,000  pounds.  Work  was  suspended  here  in  the  fall  of  1875. 

Bininger  Range.  This  range  has  Ijeen  worked  at  intervals  since  May,  1874.  It  is 
now  worked  by  Stephens,  Nankivel  &  Rowe;  four  men  are  employed,  working  -,vith  a 
horse  pump  in  the  second  opening.  During  the  present  year  the  product  has  been 
30,000  pounds. 

Big  Pump  Range.  This  range  has  been  worked  since  October  1,  1876,  by  Rich- 
ard Eustice  &  Co.  A  small  amount  of  ore  has  been  produced  from  the  first  opening. 

McCoy  Water- Wheel  Range.  Work  was  recommenced  here  about  August  1st, 
1876,  by  Rowe  &  Son,  in  the  first  opening. 

Gates  and  Eustice.  This  party  has  been  working  during  the  last  year  and  a  half 
on  a  range  200  feet  north  of  the  west  branch  of  the  level.  The  lead  ore  is  found  in  a 
flat  sheet  in  the  second  opening.  The  opening  is  seven  feet  high  and  averages  seven 
feet  in  width.  The  sheet  is  about  one  foot  thick.  The  product  to  the  pr?sent  time  has 
been  150,000  pounds. 

Clark's  Diggings.  Two  men  have  been  working  during  the  last  year  in  the  range 
next  north  of  the  McCoy  Water- Wheel  range.  The  ore  is  found  as  "  chunk  mineral  " 
in  the  second  opening,  which  is  here  six  feet  wide.  The  product  has  been  30.000 
pounds. 

Tregenza  &  Son.  Work  was  commenced  by  this  party  in  the  fall  of  1874,  on  the 
Drybone  range,  south  of  the  Badger  lot.  The  works  are  in  the  second  opening,  which 


MINES  — HAZEL  GREEN  DISTRICT.  7uT 

is  here  from  10  to  12  feet  wide;  and  contains  a  flat  sheet  about  five  inches  thick,  of 
which  the  upper  part  consists  of  lead  ore,  and  the  lower  of  zinc  ores.  The  product  has 
boen,  zinc  ores  20  tons;  lead  ore  20,000  pounds.  Very  handsome  specimens  of  galenite 
coated  with  cerusite  are  obtained  here. 

W.  H.  Enstice  &  Bro.  This  party  commenced  work  in  the  fall  of  1875  at  Crawford's 
little  pump  shaft.  They  worked  in  the  second  opening  during  the  winter  of  1875-6, 
and  suspended  in  the  summer  on  account  of  water.  The  prospect  is  good  and  they  ex- 
pect to  resume  work  this  winter  (1876).  Product  10,000  pounds. 

Edwards  Estate.  On  this  land  there  are  several  old  ranges,  now  drained  by  the 
level  of  Crawford,  Mills  &  Co.,  in  which  the  following  mining  has  been  done: 

Peter  Skinner,  in  the  winters  of  1874-5  and  1875-6,  produced  100,000  pounds. 

Moffat  &  Co.,  in  the  same  seasons,  produced  80,000  pounds. 

Pierce  &  Trewather,  in  the  same  seasons,  produced  70,000.  Other  parties  in  the 
same  time,  in  small  amounts,  100,000. 

In  addition  to  the  parties  already  mentioned,  there  are,  in  the  winter  season,  usually 
about  sixty  miners  at  work  on  the  lands  of  the  Hazel  Green  Mining  Company. 

Diggings  in  the  Village  of  Hazel  Green  not  on  the  Lands  of  the  Hazel  Green 

Mining  Company. 

McBreen  &  Co.  This  is  an  east  and  west  sheet,  connected  with  a  quartering  one  avera- 
ging about  an  inch  thick,  situated  on  the  land  of  Dr.  McBreen,  on  the  N.  W.  qr.  of  Sec. 
25,  T.  1,  R.  1  W.  The  range  was  worked  in  1844,  and  the  ore  taken  out  to  the  water  lev- 
el. The  water  having  become  much  reduced  by  the  Hazel  Green  Company's  level,  work 
was  recommenced  in  1874,  since  which  time  about  55,000  pounds  of  lead  ore  have  been 
taken  out.  The  diggings  are  in  the  upper  beds  of  the  Galena  limestone,  and  not  down 
to  any  opening. 

Torneal's  Diggings.  A  short  distance  southwest  of  the  preceding  is  a  range  con- 
sisting of  twenty  parallel  crevices,  about  twenty-five  feet  apart,  and  bearing  N.  15°  E. 
Work  was  abandoned  on  them  in  1850,  and  was  recommenced  by  Mr.  Torneal  about 
eight  years  ago,  since  which  time  they  have  produced  42,000  pounds.  Considerable 
time  and  labor  have  been  expended  in  running  a  cross  drift  to  prove  the  ground  and  as- 
certain the  number  and  position  of  the  crevices.  The  distance  here  to  water  is  80  feet, 
and  the  diggings  are  in  the  upper  beds  of  the  Galena  limestone. 

Rowe  and  Vivian.  This  was  formerly  known  as  the  Chizzem  range,  and  is  situated 
on  Edward  Williams'  land,  in  the  southwest  quarter  of  Sec.  25,  T.  1,  R.  1  W.,  in  the 
southern  part  of  the  village  of  Hazel  Green.  It  is  a  north  and  south  range,  and  was 
worked  and  abandoned  in  1854.  Work  on  it  was  recommenced  by  the  present  parties 
in  November,  1873.  Since  then  it  has  produced  24,000  pounds.  The  full  thickness  of 
Galena  limestone  is  here  present,  overlaid  by  a  few  feet  of  clay  of  the  Cincinnati  group. 
The  deepest  shaft  is  106  feet,  and  the  total  length  of  drifts  is  about  190  feet.  Work 
was  suspended  here  in  the  spring  of  1875. 

Williams  &  Bro.  On  Edward  Williams'  land.  This  party  commenced  in  the  fall  of 
1875,  and  are  now  mining  in  a  range  a  short  distance  west  of  the  diggings  of  Eustice 
&  Co.,  in  the  village  of  Hazel  Green.  They  are  working  on  a  vertical  sheet,  and  have 
produced,  to  the  present  time,  20,000  pounds. 

Chandler's  Diggings.  These  diggings  are  situated  on  Mr.  Wetherbee's  land,  and 
on  the  Sulphur  lot  range.  Work  was  commenced  two  years  ago,  ar.i  continued  to  the 
present  time.  The  works  are  in  the  second  opening,  which  is  from  six  to  eight  feat 
wide,  and  contain  a  sheet  of  lead  ore  from  one  to  two  inches  thick,  and  also  large,  ir- 
regular masses  which  afford  handsome  specimens.  The  mine  has  produced  500,000 
pounds,  and  is  now  very  good. 


70S     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

Buncome  Diggings. 

The  Buncome  Diggings  form  a  sub-district  belonging  to  Hazel  Green.  They  are  sit- 
uated on  the  Galena  river  near  the  mouth  of  Bull  branch.  They  were  formerly  very 
productive  diggings,  and  a  few  parties  are  still  working  in  them.  They  are  situated  in 
the  Brown  rock,  which  is  the  lowest  bed  of  the  Galena  limestone,  and  is  here  from  twenty 
to  thirty  feet  thick;  and  extends  down  to  the  creek  bed  at  the  State  line,  where  the  top 
of  the  Blue  limestone  may  be  seen.  At  the  mouth  of  Bull  branch  the  top  of  the  Blue 
limestone  is  found  to  be  twenty  feet  above  the  bed  of  the  stream.  Mining  is  generally 
carried  on  here  by  drifting  into  the  side  of  the  hill.  An  example  of  this  is  seen  on  the 
land  of  Mr.  Gabriel  Mills  on  the  N.  W.  or.  of  Sec.  32,  T.  1,  R,  1  E.,  where  a  flat  sheet 
of  ore  was  found  on  the  top  of  the  Brown  rock,  on  which  a  number  of  short  levels  were 
run.  Mr.  Mills  is  now  engaged  in  running  a  level  on  the  top  of  the  Blue  limestone 
from  the  center  of  Sec.  32,  westward,  to  prove  the  ground  for  blende,  of  which  ore  small 
quantities  have  been  occasionally  found.  The  Buncome  ground  is  also  remarkable  as 
being  the  only  locality  in  which  native  sulphur  appears  in  sheet  form. 

Carpenter  &  Bennett.  These  parties  are  mining  on  Mr.  Mills'  land  on  the  N.  E. 
qr.  of  Sec.  32,  T.  1,  R.  1  E.,  on  the  east  side  of  the  Galena  river.  The  workings  are  as 
usual  in  the  Brown  rock,  and  produce  some  lead  ore  and  large  amounts  of  carbonate  of 
zinc  and  blende.  Exactly  how  much'  could  not  be  ascertained.  They  have  worked 
continuously  since  1872. 

Hicks,  Fiddick  &  Co.  Situated  on  the  land  of  the  Edwards  estate,  on  the  S.  W. 
qr.  of  Sec.  29,  T.  1,  R.  1  E.  The  diggings  are  about  a  half  a  mile  above  the  mouth  of 
Bull  branch,  and  are  also  earned  on  in  the  Brown  rock.  They  are  drained  by  a  level  a 
quarter  of  a  mile  long,  discharging  100  gallons  per  minute,  which  was  commenced  in 
1868.  The  ora  is  found  in  flat  and  pitching  sheets,  and  sometimes  contains  a  little 
blende  mixed  with  it.  Twelve  men  are  now  employed  here,  and  are  producing  a  large 
amount  of  Smithsomte.  Since  the  commencement  of  operations,  about  400,000  pounds 
of  lead  ore  have  been  produced. 

Gabriel  Mills  Diggings.  This  ground  is  on  the  N.  W.  qr.  of  Sec.  29,  T.  1,  R.  1  E., 
on  the  ridge  dividing  Bull  and  Hard  Scrabble  branches,  and  contained  the  large  lode 
mentioned  in  Prof.  Whitney's  report  of  1862,  on  pages  285  and  286.  The  ore  was  dis- 
covered here  in  1854,  and  has  been  worked  uninterruptedly  ever  since,  which  is  some- 
what remarkable,  as  a  single  range  seldom  continues  uniformly  productive  through  so 
many  years.  The  property  is  owned  by  Mr.  Mills,  and  is  now  being  worked  by  William, 
Thomas  and  James  Mills,  and  R.  Pierce.  The  deepest  shaft  is  130  feet  down  to  the 
brown  rock,  in  which  the  ore  is  found  in  flat  and  pitching  sheets.  The  ore  from  these 
diggings  is  always  coated  with  pyrites,  and  some  Smithsonite  is  found  associated  with  it. 

The  ground  has  produced  about  eight  million  pounds  of  lead  ore,  their  present  an- 
nual average  production  is  about  50,000  pounds,  with  no  sign  of  diminution. 

Simmons  &  Sons.  N.  E.  qr.  of  N.  W.  qr.,  Sec.  32,  T.  1,  R.  1  E.  A  very  fine 
prospect  has  recently  been  discovered  by  this  party  on  Mr.  G.  Mills'  land.  They  com- 
menced work  about  the  1st  of  September,  1876,  with  a  horse  pump.  After  sinking  a 
shaft  14  feet  deep,  a  flat  sheet  six  inches  thick  was  discovered  in  the  upper  pipe-clay 
opening.  The  sheet  consists  of  lead  ore,  blende  and  pyrites,  about  half  of  the  thickness 
being  lead  ore. 

There  are  also  several  isolated  ranges  lying  between  Hazel  Green  and  Benton,  and 
not  properly  belonging  to  either  district.  They  are  as  follows: 

Johns  &  Harvey.  On  the  N.  E.  qr.  of  Sec.  6,  T.  1,  R.  1  E.  The  range  was  struck 
in  1858,  and  was  worked  for  some  time  with  an  engine  and  pump,  and  then  abandoned. 
Work  was  recommenced  by  Messrs.  Johns  &  Harvey,  in  18697  and  they  are  now  work- 
ing on  the  natural  water-level,  at  a  depth  of  one  hundred  ancl  ten  feet  below  the  sur- 


MINES  — HAZEL  GREEN  DISTRICT.  709 

face,  in  the  middle  portion  of  the  Galena  limestone.  The  range  bears  slightly  north  of 
west,  and  makes  ore  in  tumbling  openings,  mixed  with  clay  and  detached  masses  of 
stone.  The  opening  is,  in  some  places,  twenty  feet  wide,  but  does  not  correspond  in 
geological  position  with  any  of  the  Hazel  Green  openings,  as  it  is  rather  above  them. 
Work  was  suspended  here  in  the  fall  of  1874.  Their  production  to  that  time  was 
900,000  pounds  of  lead  ore. 

Dawson's  Diggings  are  situated  on  the  S.  E.  qr.  of  Sec.  32,  T.  2,  R.  1  E.  The 
general  course  of  the  range  is  east  and  west,  but  it  is  found  to  pitch  in  various  direc- 
tions. They  are  worked  about  thirty  feet  below  the  surface,  in  the  upper  measures  of 
the  Galena  limestone.  They  were  discovered  in  1872.  Since  then  they  have  been 
worked  continuously,  and  have  produced  80,000  pounds. 

Drybone  Diggings.  S.  W.  qr.  Sec.  28,  T.  2,  R.  1  E.  Mining  for  drybone  has  now 
been  carried  on  here  by  George  Hoppenjohn  for  the  last  ten  years.  The  diggings  are 
known  as  the  "  Bone  Patch,"  and  are  very  shallow,  not  exceeding  twelve  or  fifteen  feet 
in  depth.  The  Smithsonite  occurs  in  bunches  as  float,  and  does  not  make  in  any  regu- 
lar sheet  or  opening.  The  amount  produced  is  about  50  tons  per  annum. 

Barney  Kesson's  Diggings  are  situated  about  a  quarter  of  a  mile  southwest  of  the 
preceding,  on  the  same  quarter  section.  Work  is  suspended  on  them  during  the  sum- 
mer seasons.  They  are  quite  productive  diggings  and  have  yielded  50,000  pounds  of 
lead  ore  per  annum  for  several  years. 

Anthony  &  Dixon's  Diggings.  S.  E.  qr.  Sec.  21,  T.  2,  R.  1  E.  These  diggings 
are  about  a  quarter  of  a  mile  south  of  the  village  of  Jenkinsville,  and  are  worked  alto- 
gether for  blende;  although  the  ore  contains  a  little  drybone  and  lead  ore.  They  are 
on  the  top  of  the  Blue  limestone,  on  winch  a  level  is  now  being  run,  and  is  completed  a 
distance  of  200  feet. 

The  ore  is  very  close-grained,  shows  no  regular  cleavage,  and  somewhat  resembles 
an  ore  of  iron.  It  is  remarkable  by  being  intersected  with  thin  parallel  plates  or  lam- 
inae of  galenite  lying  very  close  together,  presenting  reflecting  edges,  and  being  a  con- 
stituent part  of  the  ore. 

The  deposit  was  discovered  in  1872,  and  has  been  worked  continuously  since.  The 
production  has  been  180  tons  of  blende  and  10,000  pounds  of  lead  ore  per  annum. 

Resting,  Hines  and  others.  A  short  distance  southeast  of  the  preceding,  on  the 
same  quarter  section,  are  three  parties  at  work  on  some  dry  bone  diggings.  There  are 
here  several  quartering  ranges,  having  a  southwest  course.  The  Smithsonite  lies  from 
fifteen  to  sixty-five  feet  below  the  surface,  and  in  the  lower  measures  of  the  Galena 
limestone;  it  "makes"  in  flats,  sheets  and  pitches  without  much  regularity.  The 
ground  has  been  worked  about  ten  years  for  drybone.  The  average  annual  production 
has  been  about  225  tons. 

Spensley,  Winn  &  Co.  Situated  about  a  quarter  of  a  mile  southwest  of  Meeker 
Grove  P.  0.  The  above  parties  have  been  working  here  about  five  yeare.  The  ore  is 
found  in  an  irregular  flat  sheet  in  the  upper  pipe-clay  opening.  This  ground  1ms  been 
worked  at  intervals  during  the  last  twenty  years.  The  water  is  removed  by  a  horse 
pump.  The  production  of  the  last  two  years  is  as  follows:  1875,  blende,  300  tons,  lead 
ore,  20,000  pounds;  1876  to  October  1st,  blende,  400  tons,  lead  ore,  20,000  pounds. 

Greenwood  &  Miller.  S.  E.  qr.  Sec.  7,  T.  1,  R.  1  E.  This  is  an  east  and  west 
range,  discovered  by  Cook,  twenty  five  years  since.  The  present  parties  became  inter- 
ested in  it  in  1871.  Five  shafts  from  70  to  90  feet  deep  have  now  been  sunk,  and  two 
drifts  of  300  feet  each  have  been  run.  The  ore  is  found  here  in  a  crevice  opening, 
sometimes  twelve  feet  high.  The  width  of  the  opening  is  quite  variable,  as  it  is  crossed 
by  numerous  north  and  south  crevices,  which  usually  cause  it  to  expann  in  width. 
Bunches  of  ore  are  found  at  the  crossings,  but  no  regular  sheets.  The  water  is  removed 
from  the  ground  by  a  two  horse  pump  of  12  inch  bore,  6-feet  stroke,  which  pumps  awut 


710  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

90  gallons  per  minute.     It  is  estimated  that  the  ground  has  produced  a  million  pounds 
of  ore,  and  its  present  annual  product  is  about  300,000  pounds. 

NEW  DIGGINGS  DISTRICT. 

Considerable  lead  ore  is  now  being  raised  in  the  vicinity  of  New  Diggings,  being 
mostly  on  the  ridge  immediately  south  of  the  village.  The  following  section  taken  from 
the  mines  south  of  the  village  will  give  a  correct  idea  of  the  relative  position  of  the  sev- 
eral beds  and  openings : 

Ft.    In. 

Soil  and  clay 14 

Galena  limestone 60 

Flint  bed 1      2 

Shale 2 

First  opening  (sometimes  called  crevice  opening) 5 

Limestone  cap 2 

Second  opening  (sometimes  called  flat  opening) 5 

Flinty  rock 9 

Third  opening  (this  is  the  principal  flat  opening) 4 

Galena  limestone 4 

"  Putty  bed." 3 

Galena  limestone 1      8 

Fourth  opening 6 

Galena  limestone 50 

Flint  opening 3 

Brown  rock  to  top  of  Blue  limestone 13 

Total..  .  178      3 


Champion  Diggings.  N.  E.  qr.  Sec.  26,  T.  1,  R.  1  E.,  on  the  New  Diggings  ridge 
There  are  several  ranges  here  having  a  general  east  and  west  course,  one  of  which, 
known  as  Champion's  old  lode,  has  probably  yielded  more  than  any  single  range  in  the 
Lead  region.  This  and  the  other  ranges  owned  by  Mr.  Champion  are  drained  by  a 
level  half  a  mile  long.  This  was  completed  in  the  year  1865,  at  an  expense  of  about 
seventy  thousand  dollars.  It  then  drained  the  ground,  and  in  four  years,  with  the  labor 
of  eight  men,  5,000,000  pounds  of  ore  were  taken  out,  which  sold  for  about  $500,000. 
This  ore  was  contained  in  an  immense  opening,  in  some  places  forty  feet  wide  by  twenty- 
five  feet  high.  This  principal  opening  is  now  worked  out,  but  the  range  still  continues 
productive,  and  has  been  worked  uninterruptedly  for  the  last  ten  years.  Average  pro- 
duct per  year,  85,000  pounds. 

Work  is  now  being  carried  on  south  of  the  old  ranges,  at  the  western  end,  in  the 
Myers  lot;  a  shaft  has  been  sunk  seventy- three  feet  to  the  first  opening,  which  is  here 
about  10  feet  high,  and  from  20  to  30  feet  wide.  There  are  here  three  parallel  crevices, 
one  of  which  is  about  8  feet  wide.  Seventeen  men  are  now  employed  in  the  Champion 
Diggings.  Mining  is  carried  on  continuously,  and  the  annual  product  is  about  200,000 
pounds. 

Craig  Diggings  are  situated  on  the  New  Diggings  ridge  on  the  N.  E.  qr.  of  Sec. 
26  and  N.  W.  qr.  Sec.  25,  T.  1.  R.  1  E.  There  are  here  three  principal  east  and  west 
ranges,  a  few  feet  apart.  The  one  which  is  now  worked  is  known  as  the  Simpson  Pump 
range.  These  ranges  were  discovered  in  1834.  In  the  spring  of  1874,  a  shaft  was  sunk 
on  one  of  them,  and  they  are  now  worked  in  the  second  opening.  They  produce  only 
lead  ore,  found  in  a  flat  opening  which  is  100  feet  wide,  and  has  been  worked  to  a  length 


MINES  — NEW  DIGGINGS  DISTRICT.  7H 

of  150  feet.  They  are  worked  only  in  the  whiter;  and  produce  40,000  pounds  per 
annum. 

Craig,  Sanders  and  Campbell.  Work  was  commenced  by  this  party  in  the  fall 
of  1874,  on  the  east  end  of  the  Simpson  Pump  range.  Tha  mining  is  carried  on  in 
the  first  opening.  The  product  has  been  258,000  pounds,  the  greater  part  of  which  was 
produced  this  year  (18T6).  The  extreme  west  end  of  this  range  has  been  worked  by 
Craig,  Stephens  &  White,  during  the  past  year,  but  has  not  yet  produced  anything. 

Craig  Level  Company.  A  company  consisting  of  several  persons  residing  in  New 
Diggings  and  the  adjacent  towns,  and  representing  an  extensive  capital,  have  been  en- 
gaged for  several  years  in  running  a  level  on  the  south  side  of  the  New  Diggings  ridge, 
for  the  purpose  of  unwatering  the  extensive  east  and  west  ranges  on  and  near  the  sum- 
mit of  the  ridge.  It  is  already  so  far  advanced  that  it  has  lowered  the  water  in  the 
mine  several  feet,  sufficient  to  admit  of  the  production  of  enough  lead  ore  to  more  than 
defray  its  expenses.  Mining  is  now  carried  on  on  Pump  range,  the  Mitchell  range,  and 
several  others;  the  company  are  making  several  "crosscut  drifts  "  for  the  purpose  of 
prospecting  their  ground.  The  following  are  the  principal  mining  operations  now 
(Oct.,  1876)  in  progress  here. 

On  the  ground  owned  by  Mr.  Craig  there  are  two  men  working  the  level;  two  men 
working  south  on  a  cross  cut  from  the  pump  shaft  range;  and  two  men  working  a  cross 
cut  north  from  the  same  range. 

On  the  ground  owned  by  Mr.  March  are  four  men  working  westward,  and  producing 
lead  ore  from  the  pump  shaft  range,  and  two  men  working  a  cross  cut  from  the  same 
range  southward. 

On  the  ground  owned  by  Mr.  Bird  there  are  four  men  prospecting  on  the  eastern  part 
of  the  Mitchell  range,  and  four  men  working  on  an  opening  of  that  range,  raising  ore; 
also  two  parties  of  three  men  each  prospecting  on  the  east  end  of  the  pump  shaft  range. 

On  the  Dutch  lot  are  two  men  drifting  from  the  Mitchell  range  southward;  two  men 
cross  cutting  from  the  same  range  northward;  three  men  working  westward  on  the 
range,  and  producing  ore;  two  men  working  a  sheet  of  ore  on  a  north  and  south  range. 

On  the  ground  owned  by  Craig  and  Dunlap  are  three  men  working  an  old  east  and 
west  range  on  the  ridge;  and  three  men  prospecting  and  raising  ore. 

The  mining  operations  of  the  Craig  Level  company  have  been  very  productive  of  lead 
ore.  The  amounts  produced  previous  to  1874  could  not  be  ascertained.  During  the 
year  1873  it  was  70,000  pounds,  and  from  March,  1874,  to  October  1,  1876,  the  product 
was  2,075,470  pounds. 

Brown,  Dodge  &  Co.  This  party,  consisting  of  four  men,  have  been  working  on 
the  west  end  of  the  Mitchell  range,  on  land  owned  by  Col.  S.  Scales.  The  product  has 
been  10,400  pounds,  all  raised  within  the  last  year. 

Harper,  Hird  &  Co.  Situated  on  the  New  Diggings  ridge,  a  short  distance  west  of 
the  Craig  diggings,  on  two  east  and  west  ranges,  known  respectively  as  the  Wiley  and 
Engine,  on  which  the  water  has  been  reduced  about  four  feet  by  the  Craig  level.  They 
were  quite  large  ranges,  and  were  extensively  worked  many  years  since.  Work  was  re- 
sumed on  them  by  the  above  parties  in  February,  1873.  Since  then,  the  product  has 
been  303,000  pounds.  The  crevice  of  the  Engine  range  is  here  about  three  feet  wide, 
and  the  ore  makes  in  the  first  opening;  while  on  the  Wiley  range  the  crevice  is  ten 
feet  wide,  and  the  ore  makes  in  the  crevice  and  not  in  the  opening.  The  ground  is 
owned  by  Col.  Sam.  Scales,  and  four  men  are  employed. 

The  existence  of  lead  and  zinc  ore  in  the  upper  pipe-clay  opening  (upper  surface  of 
the  Blue  limestone)  is  also  known  at  New  Diggings.  A  mining  company,  known  as 
the  Occidental,  was  in  operation  in  1873,  by  whom  a  level  had  been  run  on  this  open- 
ing, which  resulted  in  the  discovery  of  a  flat  sheet  of  blende  or  lead  ore.  No  work  has 
been  done  here  recently,  but  the  prospect  is  considered  good. 


712  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

Catehall  Diggings.  N.  W.  qr.  Sec.  30,  T.  1,  R.  2  E.  These  diggings  have  in 
former  years  produced  large  quantities  of  ore;  exactly  how  much  could  not  be  ascer- 
tained. After  lying  idle  for  some  years,  work  was  resumed  on  them  in  1870,  by  S.  and 
C.  Vickers,  J.  and  T.  Peacock  and  John  Henry.  They  were  worked  for  a  year  with  a 
horse-pump,  and  after  that  with  a  steam-pump,  the  former  having  been  insufficient  to 
remove  the  water.  There  are  here  two  north  and  south  ranges  crossed  by  several  east 
and  west  ranges,  which  produced  blende  and  lead  ore.  The  pump-shaft  is  located  on 
one  of  these  crossings,  and  is  48  feet  deep.  A  series  of  levels  was  run  from  here  to  the 
New  Diggings  ridge  by  which  it  was  ascertained  that  the  top  of  the  ridge  was  on  a  level 
with  the  bottom  of  the  shaft;  which  shows  that  the  openings  existing  at  this  place  are 
above  those  at  New  Diggings,  and  probably  near  the  middle  of  the  Galena  limestone. 
The  Catehall  diggings  ceased  being  worked  in  January,  1873.  The  pump  and  engine 
still  remain  on  the  ground.  The  product  during  the  three  years  of  working  is  said  to 
have  been  two  million  pounds. 

Howe  &  Alderson.  S.  E.  qr.  Sec.  15,  T.  1,  R.  1  E.  This  ground  is  situated  a  short 
distance  north  of  the  Democrat  furnace,  and  belongs  to  the  Leakley  estate.  The 
range  was  discovered  and  worked  about  1847,  and  work  was  resumed  on  it  by  the  pres- 
ent parties  about  fourteen  years  since  (1862).  The  general  course  of  the  range  is  east 
and  west;  the  extent  of  the  drifts  is  from  300  to  400  feet,  in  the  course  of  which  five 
flat  openings  and  one  crevice  opening  have  been  found.  The  flat  openings  are  not  far 
above  the  Blue  limestone.  There  are  eight  shafts  going  down  to  the  openings,  from  30 
to  80  feet  deep.  The  ore  is  generally  small  with  wash-dirt,  but  little  large  or  "  chunk- 
mineral  "  is  found.  The  diggings  are  entirely  free  from  water.  During  the  past  four- 
teen years  they  have  produced  about  1,000,000  pounds.  Work  was  suspended  here 
about  January  1,  1876. 

John  Rain  &  Co.  S.  E.  qr.  Sec.  31,  T.  1,  R.  1  E.  The  land  is  owned  by  Messrs. 
Hodge  &  Scales  and  the  Field  estate.  The  course  of  the  range  is  N.  5°  E.  It  is  known 
as  the  Raspberry  range,  from  the  name  of  the  man  who  discovered  it  in  1849,  and  some- 
times as  the  Dinsell  range.  The  workings  are  all  in  the  first  of  the  New  Diggings 
opening,  although  the  second  has  also  been  reached.  There  are  five  shafts  down  to  the 
opening,  and  about  500  feet  of  drift.  The  opening  is  quite  variable  in  size,  and  is 
sometimes  as  much  as  thirty  feet  wide.  The  ore  occurs  as  wash-dirt,  although  large 
pieces  are  occasionally  found.  The  diggings  have  been  worked  for  lead  ore  during  the 
last  seven  years,  since  which  time  Messrs.  Rain  &  Co.  have  taken  out  as  follows:  1871, 
50,000  pounds;  1872,  100,000;  1873,  75,000;  1874,  75,000.  The  product  for  1875-6  was 
not  learned,  but  the  mine  is  now  productive. 

Diggings  on  the  Leakley  Estate. 

Robbins  &  Bros.  Four  men  have  been  employed  here  during  the  last  year,  work- 
ing an  east  and  west  range  with  a  horse  pump.  The  amount  raised  is  not  known,  but 
it  is  understood  that  the  ground  yields  enough  ore  to  pay  good  wages. 

Hall  &  Rain.  S.  E.  qr.  Sec.  23,  T.  1,  R.  1  E.  This  is  a  new  east  and  west  range 
on  the  Leakley  estate,  discovered  in  1873.  The  ore  occurs  in  a  crevice  opening  from  40 
to  45  feet  below  the  surface.  Four  shafts  have  been  sunk  in  it,  and  one  drift  run  a  dis- 
tance of  400  feet.  About  119,000  pounds  have  been  produced  since  they  were  discovered. 
Work  was  suspended  this  year  (1876). 

E.  Ashworth  Diggings.  S.  E.  qr.  Sac.  24,  T.  1,  R.  1  E.  This  is  an  east  and  west 
range  on  the  Leakley  estate,  discovered  in  the  fall  of  1873.  The  workings  at  this  place 
are  confined  by  water  to  the  first  opening,  which  is  here  crossed  by  numerous  quartering1 
swithers  from  four  to  six  feet  apart.  The  crossings  are  the  most  productive  parts  of  the 
opening,  and  the  ore  frequently  comes  up  to  the  surface  clay.  At  the  time  they  wero 
visited,  June,  1874,  five  shafts  had  been  sunk  about  35  feet  deep;  one  of  the  drifts  was 


MINES  — SHULLSBURG  DISTRICT.  713 

about  100  feet  long,  and  there  were  several  of  50  feet  each.  The  product  to  that  time 
was  4,000  pounds  of  lead  ore,  and  fifteen  tons  of  drybone.  They  have  been  working 
continuously  since,  producing  small  amounts. 

Phoenix  Lead  Mining  and  Smelting  Co.  Sec.  13,  T.  1,  R.  1  E.  A  great  deal  of 
mining  has  been  earned  on  here  since  a  very  early»day,  and  the  ground  has  been  very 
productive  of  ore.  The  principal  vein,  which  is  known  as  the  Ellis  sheet,  was  discov- 
ered by  a  miner  of  that  name,  about  thirty-five  years  since  Its  course  is  N.  20°  E., 
and  it  has  been  worked  for  a  distance  of  about  half  a  mile.  The  workings  so  far  have 
been  confined  to  the  Galena  limestone,  of  which  there  is  a  thickness  of  150  feat  at  the 
pump  shaft,  at  the  summit  of  the  ridge.  This  shaft  has  been  sunk  to  a  depth  of  115 
feet,  leaving  thirty-five  feet  of  the  formation  unexplored,  exclusive  of  the  underlying 
Trenton  limestones,  which  have  here  a  thickness  of  about  fifty  feet.  The  sheet  of  ore 
is  nearly  perpendicular,  and  varies  from  two  to  eighteen  inches  in  thickness  as  deep  as 
the  shafts  were  sunk.  The  same  system  of  surface  mining  obtained  here  as  at  other 
places,  by  means  of  which  the  ore  was  extracted  down  to  the  natural  water  level  but  a 
short  distance  below  the  surface,  leaving  the  main  body  of  ore  untouched.  In  this  man- 
ner more  than  2,500,000  pounds  of  lead  ore  were  obtained.  In  the  year  1865  a  level 
was  commenced  with  a  view  to  drain  the  ground,  and  was  prosecuted  with  slight  inter- 
mission until  1872.  Its  present  length  is  1 ,700  feet,  and  when  completed  it  will  drain  the 
ground  to  a  depth  of  135  feet.  Several  other  large  east  and  west  ranges  traverse  this 
ground,  among  which  are  the  Bobineau,  and  the  Dowd  &  McGinnis,  on  the  W.  hf .  of 
the  S.  E.  qr.  of  Sec.  14,  T.  1,  R.  1  E.,  which  have  yielded  heretofore  not  lass  than  threo 
million  pounds. 

SHULLSBURG  DISTRICT. 

StopHne  Diggings.  The  property  is  situated  on  the  N.  W.  qr.  of  Sec.  28,  N.  E.  qr. 
of  Sec.  29  and  S.  E.  qr.  of  Sec.  20,  all  in  T.  1,  R.  3  E.  Although  the  mine  is  not  in 
operation,  it  is  in  a  condition  to  be  worked  on  very  short  notice. 

The  following  information  in  regard  to  it  was-  obtained  from  the  owner,  Mr.  Edward 
Meloy,  and  personal  inspection  of  the  ground.  Nearly  if  not  quite  the  entire  thickness 
of  Galena  limestone  is  present  at  this  locality.  The  northern  outcrop  of  the  Cincinnati 
group  is  found  about  a  mile  to  the  southwest.  The  pump  shaft  has  been  sunk  in  a 
natural  chimney  to  a  depth  of  112  feet  below  the  surface,  and  has  now  reached  what  is 
known  as  the  green  bed  or  cap  of  the  Shullsburg  openings.  The  water  was  removed  by 
an  engine  and  lifting  pump  discharging  500  gallons  per  minute.  All  the  water  came 
up  in  the  shaft  through  the  chimney.  While  the  pump  was  in  operation,  two  springs 
situated  respectively  one-half  mile  east  and  northwest  of  the  shaft  ceased  to  flow. 
There  are  two  principal  ranges  here,  one  baaring  N.  30°  E.  from  the  pump  shaft  and 
worked  for  a  distance  of  800  feet  northeast  of  the  shaft,  and  the  other  bearing  N.  10°  E, 
about  140  feet  west  of  the  shaft  worked  about  500  feet,  connected  by  a  quartering  range 
running  north  of  east. 

These  ranges  were  struck  in  1863,  and  worked  until  1869,  and  are  thought  to  be  a 
continuation  of  the  Shullsburg  elevator  ranges.  Two  shafts,  sunk  on  the  range,  bear- 
ing N.  30°  E.,  have  turned  out  1,000  pounds  to  the  foot  without  any  drifting  and  the 
whole  tract  within  an  area  which  would  be  embraced  within  three  acres  of  ground  had 
produced  about  600,000  pounds.  In  every  shaft  from  which  ore  has  been  raised,  the  in- 
dications of  large  bodies  below  are  very  strong, 

A  very  peculiar  formation  was  found  in  sinking  on  the  N.  30°  E.  range.  Commenc- 
ing at  a  depth  of  35  feet  from  the  surface,  a  hard  brecciated  limestone  sets  in,  filled 
with  pyrites,  and  in  some  cases  with  galenite;  this  formation  continues  as  deep  as  the 
shafts  were  sunk.  This  was  not  found  on  other  ranges  in  this  locality,  and  is  a  mode 
of  occurrence  peculiar  to  one  range. 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


FIG.  17. 


VKIN-STONB  BBECCIA,  STOPLINE  DIGGINGS. 


The  breccia  consists  of  small, 
angular  pieces  of  Galena  lime- 
stone, similar  to  the  adjacent 
rock  of  the  formation.  It  ap- 
pears to  have  been  caused  by 
the  undermining  and  falling  in 
of  a  portion  of  the  formation, 
by  a  previous  subterranean 
drainage.  The  rubbing  and 
grinding  of  the  sides  of  the  fis- 
sure against  each  other  in  the 
course  of  the  movement  broke 
oft'  pieces  of  various  sizes,  and 
the  interstices  and  cavities  were  subsequently  filled  with  pyrites. 

McNulty  Mine.  In  June,  1873,  work  was  recommenced  on  these  old  ranges,  and- 
considerable  capital  expended  in  erecting  new  machinery  and  buildings,  the  old  ones 
having  been  previously  burned.  It  is  now  owned  and  operated  by  Messrs.  J.  M.  Ryan, 
of  Galena,  and  M.  A.  Fox,  of  Shullsburg. 

The  mine  is  situated  on  the  N.  E.  qr.  of  the  N.  E.  qr.  of  Sec.  15,  T.  1,  R.  2  E.,  a 
short  distance  south  of  the  village  of  Shullsburg.  There  is  here  a  thickness  of  about  200 
feet  of  Galena  limestone,  or  four-fifths  of  the  entire  formation.  The  ore  is  obtained  in 
the  usual  opening  common  to  all  the  mines  of  the  Shullsburg  district,  between  what  aro 
known  as  the  green  and  clay  beds,  of  which  the  green  bed  is  regarded  as  the  top  and 
the  clay  bed  as  the  bottom  of  the  opening.  In  this  mine  the  following  stratigraphical 
information  was  obtained:  Five  feet  below  the  clay  bed,  and  150  feet  below  the  sur- 
face is  an  opening,  and  a  bed  of  white  rock  two  feet  thick,  then  a  layer  of  hard  gray 
rock  three  feet.  Below  this  was  found  a  flat  sheet  of  galenite,  mixed  with  pyrites,  and 
indications  of  an  opening  below.  It  is  a  peculiarity  of  the  mining  ground  on  this  ridge, 
that  all  crevices  south  of  the  Shullsburg  branch  pitch  or  dip  to  the  south,  about  six 
inches  in  ten  feet,  until  the  summit  of  the  ridge  is  reached.  Here,  as  in  the  south  shaft 
of  the  McNulty,  the  crevices  are  vertical.  In  this  shaft  the  crevice  penetrates  through 
the  clay  floor,  and  continues  on  going  down,  being  the  only  crevice  which  has  done  so. 
Proceeding  further  south,  over  the  crest  of  the  ridge,  the  crevices  all  dip  or  pitch  to  the 
north.  Taken  together,  this  system  of  crevices  seems  to  present  a  fan-like  shape,  ap- 
proaching one  another  as  they  descend.  In  the  spring  of  1876,  a  new  east  and  west 
range  was  discovered  in  this  mine,  south  of  and  parallel  to  the  one  already  worked. 
It  promises  to  be  very  productive  of  lead  ore.  The  production  of  this  mine  from  June 
1,  1873,  to  March  1,  1876,  is  as  follows:  1873,  200,000  pounds;  1874,  150,000  pounds; 
1875,  75,000  pounds;  1876,  210,000  pounds. 

Rickert,  Stevens  &  Co.  These  diggings  are  situated  on  the  N.  W.  qr.  of  the  N.  "W. 
qr.  of  Sec.  14,  about  500  feet  east  of  the  McNulty  mine,  and  connected  with  it.  Their 
geological  position  in  respect  to  strata  and  openings  are  almost  the  same.  The  ore  is 
found  in  the  usual  Shullsburg  opening,  but  in  a  few  instances  it  runs  above  it  for  a  short 
distance,  and  then  drops  down  again,  presenting  a  saddle-shaped  appearance.  At  the 
south  shaft  the  rock  is  very  much  disturbed  and  broken,  apparently  in  an  area  of  about 
200  feet  in  diameter.  It  is  in  loose  masses  of  all  sizes  and  shapes,  containing  more  or 
less  ore  scattered  through  it,  and  the  fine  earthy  material  known  among  the  miners  as 
sand.  The  strata  pitch  in  every  conceivable  direction  and  degree,  from  horizontal  to 
vertical,  crevices  and  veins  cannot  be  followed  through  it  with  any  degree  of  certainty; 
but  at  the  borders  of  this  disturbed  area,  as  well  as  above  and  below  it,  the  strata  havo 
their  normal  position,  which  is  nearly  horizontal.  This  is  merely  a  local  disturbance, 
and  is  probably  due  to  the  unequal  hardness  and  solubility  of  the  formation.  Consider- 


MINES  —  SHULLSBURG  DISTRICT.  715 

able  of  the  limestone  seems  to  have  been  removed  by  currents  of  water  running  through 
the  opening,  thus  permitting  large  and  small  irregular  masses  to  fall  from  above,  and 
filling  the  interstices  with  tho  fine  insoluble  residuum  of  sand. 

In  connection  with  this  irregularity  was  noticed  a  remarkable  "chimney  "  about  36 
feet  long  by  20  feet  broad,  and  extending  upward  further  than  has  yet  been  followed. 

It  was  originally  filled  with  loose  masses  of  galenite  rock  and  sand.  In  the  ground 
on  this  ridge  the  strata  dip  on  both  sides  toward  the  north  and  south  line  between  Sees. 
14  and  15,  on  the  west  side  about  four  feet  in  a  quarter  of  a  mile,  and  on  the  east  side 
one  foot  in  thirty  rods.  The  ground  is  drained  by  a  horse-pump  into  a  level  a  short 
distance  below  the  surface.  The  mine  produces  very  handsome  cabinet  specimens  of 
galenite  and  caloite,  in  the  form  of  dog-tooth  spar. 

The  following  section  will  serve  to  convey  a  general  idea  of  the  arrangement  of  the 
strata  on  this  ridge : 

Soil  and  clay 6  to  10  feet 

Galena  limestone 100     " 

Flint  bed 4  to    8     " 

Green  bed  to  clay  bed,  including  the  opening 14  to  18     " 

Galena  limestone  to  top  of  Blue  limestone 65    " 

Total  average  thickness 195    " 


This  may  be  compared  with  the  section  taken  at  New  Diggings,  and  given  on  page 
710  of  this  report.  Reckoning  upwards  from  the  top  of  the  Blue  limestone  to  the  top  of 
the  green  bed,  or  cap  of  the  Shullsburg  opening,  the  distance  is  found  to  be  about  80 
feet,  and  in  the  New  Diggings  section,  from  the  top  of  the  Blue  limestone  section  to 
the  top  of  the  flinty  rock,  which  is  the  cap  of  the  third  or  main  opening,  the  distance  is 
82  feet. 

This  establishes  an  identity  of  geological  position  of  these  two  points.  Measuring 
downward  from  the  cap  in  the  Shullsburg  opening,  its  average  distance  is  found  to  be 
sixteen  feet  to  the  bottom  of  the  opening.  In  the  New  Diggings  section  the  same  dis- 
tance includes  all  that  lies  between  the  top  of  the  third  and  bottom  of  the  fourth  open- 
ing, and  finally  each  is  underlaid  by  about  the  same  thickness  of  unproductive  rock. 
The  correspondence  between  these  openings  is  thus  very  distinctly  marked.  The  un- 
productive beds  in  the  New  Diggings  openings  seem  to  disappear  on  going  eastward, 
and  finally  the  openings  unite  on  reaching  Shullsburg. 

In  regard  to  the  production  of  these  diggings,  it  is  estimated  that  the  S.  hf.  of  Sec.  10, 
and  the  N.  W.  qr.  of  the  N.  W.  qr.  of  Sec.  14,  being  an  area  of  one  mile  long  on  a 
course  S.  70°  E.,  and  three-quarters  of  a  mile  wide,  including  the  McNulty  and  Rick- 
ert's  diggings,  have  produced  since  the  commencement  of  mining  operations  not  less 
than  100,000,000  pounds. 

The  preceding  information  in  regard  to  the  mine  of  Rickert,  Stephens  &  Co.  was  ob- 
tained at  the  time  I  examined  them  in  June,  1873.  Since  then  I  have  recently  received 
the  following  information  concerning  them  from  Mr.  John  E.  Hoover,  of  Shullsburg,  to 
whom  I  am  also  indebted  for  valuable  information  relative  to  the  Irish  Diggings  and 
the  McNulty  mine : 

"  The  bearing  of  the  crevice  on  which  we  (Rickert,  Stephens  &  Co.)  are  now  working 
is  due  east  and  west.  The  mineral  is  found  about  12  feet  below  the  green  bed  or  cap, 
and  is  mixed  with  sulphur  (pyrites).  The  rock  is  different  from  any  before  taken  out  of 
the  mines  in  this  section.  It  is  a  dark  blue,  and  mixed  with  sulphur  and  flint,  and  is 
very  hard.  In  the  opening  there  is  copper  rust  or  verdigris  mixed  with  large  balls  of 
sulphur.  Dog-tooth  spar  or  tiff  is  also  found  in  large  quantities,  most  of  which  is 
attached  to  the  mineral. 


716  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

"The  company  commenced  work  in  1849,  and  on  the  present  range  in  May,  1874. 
They  are  now  operating  a  steam  pump  on  what  is  supposed  to  be  a  continuation  of  the 
South  digging  range.  The  product  from  June  1,  1873,  to  March  1,  1876,  is  as  follows: 
1873,  377,120  pounds;  1874,  201,966  pounds;  1875,  318,690  pounds;  1876,  153,720 
pounds.1' 

Siiverthorn  Mine.  N.  W.  qr.  Sec.  32,  N.  E.  qr.  Sec.  31,  T.  2,  R.  2  E.  The  great- 
est thickness  of  Galena  limestone  found  on  the  ridge  was  about  one  hundred  feet.  The 
ground  is  drained  by  a  level  run  in  the  carbonaceous  shale,  on  the  top  of  the  Blue 
limestone,  which  has  here  a  very  great  thickness,  being  nowhere  less  than  two  feet,  and 
in  some  places  seven  and  a  half  feet  thick.  It  seems  in  this  mine  to  replace  the  pipe- 
clay opening.  It  is  very  easy  to  work,  and  consequently  this  level  has  been  compara- 
tively inexpensive.  This  shale,  when  dried,  burns  with  a  bright  yellow  flame  and  much 
smoke  until  the  carbon  is  exhausted,  but  owing  to  the  amount  of  calcareous  matter  it 
contains,  it  is  not  much  reduced  in  bulk.  These  diggings  produced  in  1871,  200,000 
pounds,  and  in  1872,  about  100,000  pounds.  Their  product  in  previous  years  could  not 
be  ascertained.  Work  was  suspended  on  them  in  1875.  An  analysis  of  lead  ore  from 
the  Siiverthorn  mine  gave  the  following  results:  Lead  sulphide,  97.06;  metallic  Lead, 
84.07;  insoluble  silicious  residuum,  1.76. 

Dry  Bone  Diggings.  Situated  on  the  S.  W.  qr.  of  the  S.  E.  qr.  and  the  S.  E.  qr. 
of  the  S.  W.  qr.  of  Sec.  4,  T.  1,  R.  2  E.  The  ranges  here  run  in  nearly  an  east  and 
west  direction.  The  diggings  are  situated  in  the  lower  strata  of  the  Galena  limestone; 
the  top  of  the  Blue  limestone  is  found  a  short  distance  down  the  stream.  Although 
shallow,  these  diggings  have  been  very  productive  of  zinc  ore,  and  are  still  successfully 
worked. 

Irish  Diggings.  Sec.  2,  T.  1,  R.  2  E.  These  diggings  have  not  been  worked  for 
many  years  on  account  of  water,  but  were  formerly  very  productive  and  were  abandoned 
with  ore  going  down  in  the  crevices.  The  greatest  thickness  of  Galena  limestone  on 
this  ground  is  about  150  feet.  They  could  be  roadily  unwatered  by  means  of  a  level 
from  some  point  on  the  Shullsburg  branch. 

Meloy  and  Fox.  In  the  early  part  of  the  year  1875,  that  part  of  the  Irish  Diggings 
known  as  the  Findlcy  Cave  range  was  leased  by  Messrs.  E.  Meloy  and  M.  A.  Fox,  of 
Shullsburg.  It  is  situated  on  the  N.  E.  qr.  of  Sec.  2,  T.  1,  R.  2  E.,  and  comprises  99 
acres  of  land,  lying  about  a  mile  northeast  of  the  village.  The  range  was  worked  du- 
ring the  months  of  April,  May  and  June,  1875,  and  in  November  of  that  year  a  steam 
engine  and  pump  were  erected,  and  it  has  been  worked  continuously  to  the  present  time 
(November,  1876).  The  pump  shaft  is  now  about  80  feet  deep.  Water  is  discharged 
into  an  adit  connecting  with  the  shaft  at  20  feet  below  the  surface,  at  the  rate  of  150 
gallons  per  minute.  The  course  of  the  vein  is  N.  7°  E.,  having  a  dip  to  the  eastward 
of  four  feet  in  one  hundred.  The  distance  between  the  walls  of  the  vein  or  crevice  va- 
ries from  two  and  a  half  to  seven  feet,  the  space  between  them  being  filled  with  the 
vein  matrix  common  to  this  neighborhood.  The  bottom  of  the  pump  shaft  is  six  feet 
below  the  top  of  the  flint  beds  (see  section  on  page  715).  The  vein  appears  to  continue 
downwards,  the  filling  of  the  crevice  being  loose  and  allowing  the  water  to  pass  readily 
through  it. 

After  sinking  the  pump  shaft,  the  vein  was  drifted  in,  a  distance  of  60  feet  to  the 
northward;  in  the  course  of  running  this  drift,  100,000  pounds  of  ore  were  extracted. 

The  foregoing  remarks  show  the  condition  of  the  mine  in  March,  1876.  The  produc- 
tion since  then  we  have  not  learned. 

This  range  was  worked  more  than  30  years  since,  with  a  two-horse  pump,  as  deep  as 
water  would  permit,  and  large  quantities  of  lead  ore  were  obtained.  These  diggings 
could  be  unwatered  to  a  much  greater  depth  by  means  of  a  level  from  some  point  on  the 
Shullsburg  Branch. 


MINES  -  BEXTOX  DISTICT.  717 

Bull  Pump  Range.  Work  is  still  carried  on,  on  this  range,  which  is  situated  on  the 
Hempstead  estate.  It  is  operated  by  Messrs.  Beebe,  of  Galena,  and  Wetherbee.  of 
Shullsburg.  The  amounts  produced  could  not  be  ascertained. 

Oakland  Mining-  Co.  The  lands  of  this  company  are  situated  in  the  S.  E.  qr.  of 
Sec.  6,  the  X.  E.  qr.  of  Sec.  5,  the  X.  W.  qr.  of  Sec.  4,  and  the  S.  E.  qr.  of  Sec.  4,  all 
in  T.  1,  R.  2  E.,  comprising  in  all  about  565  acres. 

This  ground  includes  the  old  French  range,  which  was  discovered  as  early  as  1839,  and 
produced  not  less  than  1.000,000  pounds.  It  is  connected  northward  by  some  quartering 
crevices,  and  is  known  as  the  Earnest  and  Townsend  range. 

The  thickness  of  Galena  limestone  here  is  about  170  feet.  There  are  six  shafts  on  the 
range,  averaging  about  50  feet  each.  The  lead  ore  is  abundant,  but  dips  rapidly  to  the 
northwest  beneath  the  water.  The  range  has  produced  alx»ut  400,000  pounds. 

The  ground  is  susceptible  of  drainage  from  the  Shullsburg  branch.  It  is  not  worked 
at  present. 

The  company  also  has  a  level  nearly  completed  in  the  S.  E.  qr.  of  Sec.  4,  which  is 
run  on  the  stratum  of  carbonaceous  shale,  or  the  top  of  the  Blue  limestone.  At  the 
working  shaft  there  is  a  thickness  of  90  feet  of  Galena  limestone,  of  which  the  follow- 
ing section  is  given : 

Feet. 

Clay  and  soil 18 

Yellow  flinty  limestone •    16 

Galena  limestone  containing  calcite 20 

Blue  sandy  limestone  cap 6 

Red  ochery  clay  with  lead  ore  in  flat  sheets  at  top  and  bottom,  also  dif- 
fused through  the  mass  forming  wash-dirt 12 

Unexplored  beds 18 

Total  thickness 90 

Considerable  mining  has  been  done  in  former  years  in  the  Blue  sandy  limestone  mem- 
ber of  the  section,  but  the  main  opening  appears  to  be  in  the  red- ochery  clay  which  un- 
derlies it,  which,  so  far  as  explored,  has  been  found  to  have  a  thickness  of  about  twelve 
feet,  and  to  contain  a  flat  sheet  of  galenite  nearly  continuous,  and  of  variable  thickness, 
sometimes  furnishing  pieces  of  500  pounds  weight. 

The  bearing  of  the  sheet,  so  far  as  has  been  determined,  is  west  of  north  and  east  of 
south,  with  a  slight  dip  to  the  southwest.  Its  area  has  not  been  determined,  but  so  far 
as  has  been  worked  there  are  no  indications  of  the  opening,  contracting  or  closing  up. 

BEXTOX  DISTRICT. 

In  the  immediate  vicinity  of  the  village  of  Benton,  there  are  several  parties  perma- 
nently engaged  in  mining,  besides  others  who  mine  only  in  the  winter.  The  diggings 
are  in  the  lower  beds  of  the  Galena  limestone,  yet  not  so  low  as  the  brown  rock. 

The  mode  of  occurrence  of  the  openings  in  this  vicinity  is  quite  remarkable,  and  is  as 
follows :  There  are  numerous  well  defined  north  and  south  and  east  and  west  crevices, 
which  are  followed  down  with  shafts  until  the  random  of  the  openings  is  reached.  At 
this  point,  instead  of  the  crevice  leading  into  and  being  connected  with  the  openings,  as 
is  usually  the  case,  the  crevice  usually  closes  up,  and  it  is  necessary  to  drift  at  right  an- 
gles with  the  crevice  for  a  distance  of  from  ten  to  fifteen  feet  on  each  side,  where  the 
openings  are  usually  found.  The  annexed  diagram  illustrates  the  relative  position  of 
ihv  openings.  A  represents  the  vertical  crevice  on  which  the  shafts  are  sunk.  The  dis- 
tance from  the  surface  to  the  top  of  the  first  opening  is  from  five  to  fifty  feet,  according 
to  the  amount  of  denudation  of  the  ground.  B  B  represents  the  first  opening,  which  is 


718  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


SECTION  OF  THE  BENTON  OPENING. 


a  flat  flint  opening  four  feet  high.     C  C  represents  the  second,  which  is  also  a  flat  flint 
Opening,  four  feet  high.     D  D  represents  the  third,  which  is  not  a  flint  opening.     It 

is  about  four  feet  high , 

FIG.  18.  similar  to  B  and  C.    The 

distance  between  tl;e  first 
and  second  openings  is 
four  feet  of  unproduc- 
tive cap  rock;  between 
the  second  and  third, 
ten  feet  of  similar  rock. 
The  openings  are  about 
fifteen  feet  wide,  and 
sometimes  as  much  as 
four  hundred  feet  long. 
Having  described  the 
position  and  mode  of  oc- 
currence of  the  ore,  the 
different  diggings  now 
in  operation  will  be  de- 
scribed. 

Bainbridge  &  Vip- 
ord.  S.  E.  qr.  Sec.  8, 
T.  1,  R.  1  E.  This  is 
an  east  and  west  range 
somewhat  near  a  mile  long,  which  was  worked  about  twenty-two  years  since  and 
abandoned.  Prior  to  1854,  it  produced  about  one  and  a  half  million  pounds.  About 
seven  years  since  some  work  was  done  on  it,  and  one  million  pounds  were  produced. 
Work  was  recommenced  on  the  eastern  end  by  the  present  parties  in  February,  1874, 
and  has  continued  to  the  present  time  (November,  1876).  The  annual  product  is  about 
20,000  pounds.  During  the  last  year  and  a  half  they  have  been  worked  with  a  horse 
pump. 

Bainbridge,  Mnndy  &  Maighn.  This  is  a  quartering  southwest  and  northeast 
range,  about  100  yards  north  of  the  preceding.  This  range  was  never  worked  previous 
to  March,  1874.  It  is  now  worked  only  in  the  winter  seasons.  It  has  produced  in  all 
about  50,000  pounds.  The  ore  in  these  diggings  and  the  preceding  is  found  in  openings 
detached  from  the  main  crevice. 

Metcalf,  Harker  &  Alexander.  K.  W.  qr.  Sec.  9,  T.  1,  R.  1  E.  This  ground  is 
situated  on  what  is  known  as  the  Swindler  ridge.  It  derived  its  name  from  the  custom 
which  formerly  existed  among  the  miners  of  cutting  through  and  breaking  into  each 
other's  ground  to  steal  the  ore,  which  the  complicated  nature  of  the  openings  enabled 
them  to  do.  This  range  was  struck  in  1871,  and  has  been  worked  continuously  ever 
since.  The  depth  to  the  top  of  the  first  opening  is  fifty  feet  at  this  shaft,  and  on  the 
ridge  generally,  although  the  opening  is  said  to  dip  slightly  to  the  west.  Some  water 
is  encountered  on  the  ridge,  and  the  present  parties  have  found  it  necessary  to  work  a 
two-horse  pump.  The  production  to  November  1,  1876  has  been  600,000  pounds. 

Bainbridge  Diggings.  Situated  on  the  E.  hf.  of  the  N.  E.  qr.  of  Sec.  4,  T.  1,  R. 
1  E.  Work  was  commenced  here  by  Mr.  Thomas  Bainbridge,  of  Benton,  in  the  winter 
of  1874.  In  May,  1875,  an  irregular  deposit  of  lead  and  zinc  ore  was  discovered  about 
fifty  feet  below  the  surface,  having  a  course  a  little  west  of  south.  Three  men  are 
usually  employed.  Its  production  has  been  25  tons  of  Smithsonite  and  25,000  pounds 
of  lead  ore. 

Harvey's  Diggings.    Situated  on  the  same  ground,  and  about  250  yards  northwest 


MINES—  PLATTEVILLE  DISTRICT.  719 

of  the  preceding.  Work  was  begun  here  in  the  winter  of  1875-6,  and  a  large  flat 
sheet  of  Suiithsonite  was  discovered,  which  has  been  worked  over  200  feet  in  diameter 
without  reaching  unproductive  ground.  It  is  found  about  50  feet  below  the  surface  in 
the  random  or  horizon  of  the  flat  flint  openings.  The  ore  is  found  in  flat  sheets  inter- 
stratified  with  the  formation.  One  hundred  tons  have  been  produced. 

McElroy  Bros.  Situated  half  a  mile  south  of  the  village  of  Benton.  This  is  a 
new  discovery,  made  in  the  winter  of  1875-6.  An  irregular  flat  sheet  of  Smithsonita 
was  found  at  a  depth  of  50  feet  below  the  surface,  from  which  in  two  months,  15 
tons  of  ore  were  produced.  Work  was  then  discontinued  during  the  summer.  The 
above  parties  intend  to  work  it  again  in  the  winter. 

M.  J.  Williams  &  Co.  Situated  on  the  S.  W.  qr.  of  the  S.  W.  qr.  of  Sec.  3,  T.  1, 
R.  1  E.  A  large  flat  sheet  of  lead  ore  and  blende,  about  one  foot  thick,  was  discovered 
in  July,  1876,  in  the  bed  of  Fever  river,  soon  after  a  heavy  flood  which  took  place  at 
that  time.  It  lies  on  the  upper  surface  of  the  Blue  limestone,  and  on  account  of  its  sit- 
uation in  the  river,  but  little  has  been  done  with  it.  It  is  an  excellent  prospect,  and 
will  doubtless  be  remunerative,  as  soon  as  the  water  can  be  removed. 

McCaffery,  Smith  &.  Co.  In  the  middle  of  October,  1876,  these  parties  commenced 
work,  sinking  a  shaft  on  the  west  line  of  the  forty  of  M.  J.  Williams  &  Co.  They  found 
the  same  sheet  of  ore  as  there  described.  In  the  space  of  two  weeks  they  had  developed 
a  fine  prospect,  and  had  produced  about  one  ton  of  ore. 

Level  Company.  On  the  N.  W.  qr.  of  Sec.  29,  T.  1,  R.  1  E.,  a  level  is  now  being 
run  by  Messrs.  Stevens,  Mason.  Miller.  Robbins,  Broderick,  Hoover,  Thompson,  Coltnian 
and  Farley,  who  own  and  have  leased  one  hundred  and  thirty-five  acres  in  Sees.  20,  21, 
28  and  29.  The  level  was  commenced  in  the  spring  of  1870,  and  has  now  reached  a 
length  of  one  thousand  feet.  It  is  being  driven  on  a  flint  opening  near  the  top  of  the 
Brownrock,  which  is  here  about  fourteen  feet  above  the  Blue  limestone. 

The  object  of  driving  the  level  is  to  unwater  the  Drummond  range,  which  runs  east 
and  west,  and  is  supposed  to  be  a  continuation  of  the  Craw  range  of  Hazel  Green,  and 
the  Nagle  range  of  Is'ew  Diggings.  It  is  believed  that  when  the  level  is  completed  it 
will  unwater  the  Drummond  range  to  a  depth  of  forty  feet  below  the  present  water 
level. 

The  level  now  gives  access  to  two  openings  in  working  it,  and  had,  when  visited,  an 
inch  sheet  of  lead  ore  in  the  working  forehead.  It  may  be  remarked  that  these  open- 
ings are  lower  than  any  of  the  Benton  openings,  and  seem  to  be  identical  with  those  of 
the  Buncome  district.  The  product  has  been  up  to  the  present  time  60,000  pounds. 

PLATTEVILLE  DISTRICT. 

The  diggings  of  the  Platteville  district  comprise  those  situated  in  the  immediate  vi- 
cinity of  the  village,  the  Whig  diggings  and  the  Big  Patch  diggings.  The  mines  near 
Platteville  are  all  included  in  Sees.  9, 10,  14  and  15;  and  of  these,  the  ones  chiefly  worked 
are  situated  on  Sees.  9  and  10,  a  short  distance  north  of  the  village.  The  diggings  here 
are  very  shallow;  the  deepest  shafts  are  seldom  more  than  thirty  feet.  The  ore  occurs 
in  bunches,  pockets  and  small  openings  in  the  clay  crevices,  and  often  comes  up  to  the 
surface.  Their  geological  position  is  about  the  middle  of  the  Galena  limestone.  There 
are  no  large  companies  at  work  in  this  district,  all  the  mining  being  done  by  parties  of 
two  or  three  persons.  There  are  quite  a  large  number  of  such  parties,  who  form  the  ag- 
gregate production  of  the  district.  A  few  of  the  more  prominent  are  here  given,  and 
their  annual  production  as  nearly  as  could  be  ascertained. 

Stevens  &  Kowe 40,000  Ibs. 

Lane  &  Lawton 60,000    " 

Wales  &  Rovve 50,000    " 


720  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

C.  Cornelius,  Jr 8,000  B>s. 

Thompson,  Phillips  &  Colt 12,000  " 

Wm.  Johnson 5,009  " 

Burns  &  Conley 100,000  " 

Sheppard 12,000  " 

Leonard  Coatcs 15,000  " 

Carlyle,  Hendershot  &  Co 30,000  " 

Other  sources  in  small  lots 63,000  " 

Total 395,000  Ibs. 


As  most  of  the  mining  is  done  in  the  winter,  none  of  the  above  mentioned  firms  were 
engaged  in  mining  at  the  time  the  district  was  visited,  and  we  are  unable  to  give  a  de- 
tailed description  of  the  several  mines. 

Whig  Diggings. 

This  is  a  small  group  of  east  and  west  ranges  in  the  S.  W.  qr.  of  Sec.  7,  T.  3,  R.  1 
W.,  on  the  ridge,  on  the  west  side  of  the  Platte  river,  which  properly  belongs  to  the 
Platteville  district.  More  or  less  mining  is  done  here  during  all  the  year.  The  follow- 
ing informatiou  concerning  them  was  obtained  from  parties  now  at  work  there.  The 
diggings  are  all  in  the  upper  beds  of  the  Galena  limestone.  The  principal  ranges  are  as 
follows: 

Gillis  Range.  This  is  the  longest  and  largest  range  in  the  Whig  diggings,  being 
half  a  mile  in  length.  The  shafts  are  sunk  on  it  from  thirty  to  fifty  feet  deep,  where  a 
crevice  opening  from  three  to  five  feet  high  is  found.  There  are  from  three  to  seven 
parallel  crevices,  which  were  discovered  in  1839.  Their  total  product  since  then  has 
been  about  five  million  pounds.  The  present  annual  product  is  15,000  pounds. 

Robbing  Range.  Situated  a  short  distance  north  of  the  Gillis.  It  was  struck  in 
1840,  and  produced  500,000  pounds.  Work  was  suspended  on  it,  and  resumed  in  1866 
by  Cronin  &  Stevens,  who  raised  about  300,000  pounds.  Less  work  is  now  done  on  it 
than  on  any  of  the  others. 

Duncan  Range.  Situated  150  yards  south  of  the  Gillis.  It  is  a  little  more  than  a 
quarter  of  a  mile  in  length.  T-here  are  here  two  parallel  crevices,  and  one  opening 
which  is  from  six  to  twenty  feet  high,  and  from  five  to  forty  feet  below  the  surface,  ac- 
cording to  the  contour  of  the  ground.  It  is  very  hard  ground  to  work,  as  everything 
has  to  be  timbered.  It  still  produces  a  little  lead  ore  and  a  little  Smithsonite,  exactly 
how  much  could  not  be  ascertained.  The  total  product  of  the  range  is  said  to  have 
been  one  and  a  half  million  pounds. 

The  relative  position  of  the  openings  here  is  as  follows: 

Feet. 

First  opening 6 

Unproductive  rock 9 

Second  opening 8 

Limestone  cap 9 

Third  opening,  height  not  known. 

Messersmith  Range.  This  range  is  situated  a  short  distance  south  of  the  Duncan, 
is  about  a  quarter  of  a  mile  long,  and  has  but  one  principal  crevice.  It  is  from  five 
to  thirty-five  feet  to  the  top  of  the  opening;  which  is  from  five  to  ten  feet  high.  The 
range  is  now  worked 'out  for  lead  ore,  but  still  produces  a  small  amount  of  Smithsonite. 

Missouri  Range.  Some  work  is  done  on  this  range  at  all  times.  It  is  situated  a 
short  distance  south  of  the  preceding,  and  is  about  a  quarter  of  a  mile  long.  .  It  has  one 
crevice,  and  an  opening  which  is  about  seven  feet  high.  It  has  produced  650,000 
pounds  since  it  was  discovered;  and  its  annual  yield  is  about  5,000  pounds. 


MINES  — MIFFLIN  DISTRICT.  721 

Dutch  Range.  The  range  was  discovered  in  1840,  and  has  been  worked  nearly 
every  year  since.  It  is  a  quarter  of  a  mile  long.  The  ore  is  found  in  bunches  mixed 
with  blue  clay,  in  the  first  opening,  which  is  from  fifteen  to  thirty-five  feet  below  the 
surface.  No  ore  is  found  in  the  lower  openings.  It  has  produced  in  all  200,000  pounds, 
and  its  present  annual  average  is  5,000  pounds. 

AVilkinson  and  Cronin  Range  is  a  quarter  of  a  mile  long,  and  was  discovered  in 
1868.  The  ore  is  found  partly  in  the  first,  and  partly  in  the  second  openings,  which  arc 
here  eight  feet  apart.  It  is  from  five  to  thirty  feet  from  the  surface  to  the  top  of  the 
first  opening.  There  are  here  two  ranges  which  have  produced  300,000  pounds,  and 
the  range  is  now  nearly  worked  out. 

Smith  Range.  This  differs  from  any  of  the  Whig  ranges  before  mentioned,  in  hav- 
ing its  course  north  and  south,  instead  of  east  and  west.  The  range  is  about  an  eighth 
of  a  mile  long,  and  the  distance  from  the  surface  to  the  top  of  the  opening  is  from  ten 
to  sixty  feet.  The  sheet  was  from  one  to  four  inches  thick,  and  was  worked  in  one 
place  down  to  the  Blue  limestone.  The  principal  bodies  of  ore  were  found  in  the  Brown 
rock  opening,  which  is  much  lower  than  the  general  run  of  openings  at  these  diggings. 
The  range  is  said  to  have  produced  200,000  pounds,  and  is  now  worked  out. 

Big  Patch  Diggings. 

The  greater  part  of  this  group  of  diggings  is  situated  in  section  10,  T.  2,  R.  1  W. 
The  general  course  of  the  range  is  N.  65°  West.  The  ore  is  found  here  in  crevice  open- 
ings, and  usually  in  the  first  opening.  The  following  parties  are  now  mining  here : 

Dixon  &  Coats  produced  since  February,  1876 400,000  fi>s. 

Casper  Linden  produced  since  March,  1876 25,000  " 

Tapper  &  Trowbridge  produced  during  August,  September,  and 

October,  1876 12,000  " 

Peacock  &  Co.,  annual  product 18,000  " 

Todd  &  Co.,  annual  product 10,000  " 

Haverncss  &  Co.,  annual  product 15,000  " 

Spink  &  Co.,  annual  product 20,000  " 

Hawkins,  Thomas  &  Co.  S.  W.  qr.  of  Sec.  31,  T.  3,  R.  1  W.  This  is  a  discovery 
of  the  year  1872.  The  ore  is  blende,  somewhat  mixed  with  rock,  and  occurs  in  a  flat 
sheet  on  the  upper  surface  of  the  Blue  limestone.  The  sheet  has  in  some  places  a  tlu'ck- 
ness  of  five  feet;  it  lies  in  the  bed  of  a  small  stream,  and  a  level  to  drain  it  is  partially 
completed.  About  27  tons  of  ore  have  been  produced. 

MIFFLIN  DISTRICT. 

Mining  operations  heie  are  now  chiefly  confined  to  several  parallel  ranges,  having  a 
general  northwesterly  course,  and  situated  about  half  a  mile  south  of  the  village,  in- 
cluding the  Penitentiary,  Dunbar  and  Owens  ranges.  The  ore  is  found  in  flat  sheets  on 
the  surface  of  the  Blue  limestone,  in  the  pipe-clay  opening.  Some  mining  is  also  done 
on  Sec.  10,  T.  4,  R.  IE.,  in  the  vicinity  of  the  Welsh  settlement. 

Penitentiary  Mine.  S.  W.  qr.  of  N.  E.  qr.  Sec.  34,  T.  5,  R.  1  E.  This  property  is 
owned  by  Messrs.  James,  John  and  Calvert  Spensley,  Wm.  Bainbridge,  J.  J.  Ross, 
Mrs.  Mitchell  and  N.  W.  Dean.  The  mine  was  opened  in  1842,  and  since  then  it  has 
been  very  productive,  and  has  been  worked  continuously  to  the  present  time.  The  mine 
is  drained  by  a  level  containing  a  tramway  on  which  the  rock  and  ore  are  carried  out  of 
the  mine.  Sufficient  water  is  removed  to  operate  a  large  wash  place.  The  distance 
from  the  entrance  of  the  mine  to  the,  forehead  is  about  1,700  feet.  The  average  width 
of  the  range  is  about  300  feet,  and  the  thickness  of  the  deposit  from  six  inches  to  two 
Wis.  SUB.  — 46 


722  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

feet.  Fifteen  men  are  now  employed  here,  the  average  being  about  twelve.  Previous 
to  1864,  the  mine  was  worked  chiefly  for  lead  ore,  producing  in  some  years  as  much  as 
170,000  pounds.  It  is  estimated  by  Mr.  Ross  that  it  produced  from  1862  to  1875, 
3,000,000  pounds  of  lead  ore  and  11,000  tons  of  blende.  The  production  for  1875  was, 
blende,  375  tons;  lead  ore,  55,000  pounds.  The  production  for  1876  was,  blende,  600  tons; 
lead  ore,  40,000  pounds. 

Jenkins,  Miller  &  Co.  These  parties  have  been  working  during  the  last  two  and  a 
half  years  on  the  Dunbar  range,  which  is  parallel  to  the  Penitentiary,  and  a  short  dis- 
tance north  of  it.  The  land  is  owned  by  Messrs.  Ross  &  Dean.  This  range  has  been 
worked  during  the  last  thirty  years,  and  is  drained  by  the  Penitentiary  level;  the  pres- 
ent workings  are  about  50  feet  below  the  surface.  The  company  produced  during  the 
year  1S7G,  to  October  1st,  blende.,  80  tons,  lead  ore,  8,000  pounds.  Their  annual  average 
is  blende,  80  tons,  lead  ore,  12,000  pounds. 

Rain,  Young  &  Jenkins.  These  parties  are  now  working  on  the  Blackjack  range, 
which  is  adjacent  to  the  Dunbar,  and  sometimes  connects  with  it.  The  present  works 
are  50  feet  below  the  surface.  The  ore  is  found  in  flat  sheets,  sometimes  70  feet  in. 
wvlth,  in  the  pipe  clay  opening,  the  height  of  the  opening  averaging  five  feet.  The 
annual  production  is  from  150  to  200  tons  of  blende,  and  from  10,000  to  15,000  pounds 
of  lead  ore. 

A  short  distance  northeast  of  the  Blackjack  is  the  Owens  range.  It  has  not  been 
worked  during  the  last  two  years,  but  is  considered  good  mining  ground. 

CENTERVILLE  DISTRICT. 

These  diggings  are  like  those  in  the  village  of  Highland,  in  that  they  are  ah  situated 
quite  close  together,  on  Sec.  7,  T.  6,  R.  1  E.,  on  the  hill  about  a  quarter  of  a  mile  east 
of  the  village. 

The  land  is  ah1  owned  by  Messrs.  Top,  Norndorf  &  Kroll.  The  miners  are  nearly  all 
Germans,  from  whom  the  following  information  was  extracted : 

The  diggings  were  first  worked  in  1836,  and  have  been  worked  continuously  ever 
since,  chiefly  for  lead  ore,  until  within  the  last  ten  years,  since  which  time  they  havo 
been  worked  for  zinc  ores.  The  workings  are  in  the  Brown-rock  opening,  and  lie  from 
five  to  fifty  feet  below  the  surface,  depending  on  the  amount  of  denudation.  Very  little 
trouble  is  experienced  from  water,  and  during  the  past  two  years  the  ground  has  been 
especially  dry.  The  principal  parties  working  here  are  as  follows : 

Heller  and  Parish.  These  parties  are  working  a  southeast  and  northwest  range, 
1,200  feet  long  and  600  feet  wide.  Their  annual  product  is:  Lead  ore,  100,000  pounds.; 
blende,  500  tons;  Smithsonite,  400  tons. 

John  Carter  and  Richard  Samuels.    On  the  same  range  as  the  preceding.    They 
have  worked  here  two  years,  and  are  producing  200  tons  of  Smithsonite  and  5,000  . 
pounds  of  lead  ore  per  annum.     Other  parties  and  their  annual  products  are  as  follows: 

Schock  and  Flemmer.    Blende,  200  tons  per  annum. 

Stepper  and  Mensing.    Blende,  100  tons  per  annum. 

George  Wieble.    Blende,  200  tons;  lead  ore,  15,000  pounds. 

Blue  River  Paint  Works. 

Situated  on  the  S.  W.  qr.  of  Sec.  7,  T.  6,  R.  1  E.  At  the  time  this  establishment 
was  visited,  work  had  been  suspended,  and  consequently  did  not  appear  in  as  flattering 
a  light  as  its  merits  would  probably  justify.  The  building  and  machinery  was  still 
standing,  in  a  condition  to  resume  work  without  delay. 

According  to  the  best  information  obtained,  the  paint  was  made  from  the  ocher  which 
is  quite  abundant  in  the  Centreville  diggings,  and  which  furnishes  quite  a'  number  of 
shades  of  yellow  in  its  raw  state,  and  an  additional  number  on  being  burned.  The  red 


MINES  — HIGHLAND  DISTRICT.  723 

paint,  however,  was  derived  from  the  upper  bed  of  the  St.  Peters  sandstone,  which  was 
crushed  and  washed;  the  red  coloring-  matter  being  readily  dissolved  out  by  the  water, 
from  which  it  afterwards  settled  on  being  allowed  to  stand.  The  colors  after  being 
burned  and  ground  were  ready  for  the  market.  As  many  as  fifteen  different  shades  of 
red  and  yellow  were  manufactured.  Several  tons  of  paint  were  placed  in  market,  and 
it  was  claimed  to  be  a  good  and  durable  article.  It  is  unfortunate  that  the  manufacture 
could  not  have  continued  longer,  and  its  qualities  been  more  definitely  ascertained  and 
generally  known. 

HIGHLAND  DISTRICT. 

Tlie  diggings  of  the  Highland  district  are  all  situated  within  a  short  distance  of  each 
other,  and  about  a  quarter  of  a  mile  north  of  the  village.  They  are  all  in  the  Brown 
rock,  the  lower  openings  never  have  been  proved.  Most  of  the  diggings  are  on  what  is 
known  as  the  Drybone  Hollow  range.  The  names  of  parties  mining,  and  the  present 
condition  of  their  diggings,  are  as  follows: 

Samuel  Hinderleiter  &  Sons.  On  the  S.  W.  qr.  of  Sec.  28,  T.  7,  R.  1  E.,  on  the 
Drybone  Hollow  range.  This  is  an  east  and  west  range  from  one-quarter  to  one-half 
mile  long,  and  from  two  to  three  hundred  feet  wide.  It  was  discovered  in  1846,  and 
worked  entirely  for  lead  ore.  It  is  now  divided  into  small  lots  of  which  Mr.  Hinderlei- 
ter's  is  one.  The  work  is  chiefly  confined  to  going  through  the  old  diggings  and  taking 
out  the  Smithsonite  left  by  former  miners,  no  blende  being  found.  The  shafts  are 
about  twenty-five  feet  deep,  which  brings  them  to  the  top  opening,  three  feet  in  height. 
The  ore  is  found  in  a  flat  sheet,  about  a  foot  thick,  with  ocher  and  clay  above  and  be- 
low it.  But  little  water  is  found  here.  The  annual  product  of  this  lot  is  about  thirty 
tons  of  Smithsonite. 

3Iulligan  &  Francis.  These  parties  have  diggings  in  all  respects  similar  to  those 
already  described,  on  a  lot  about  150  feet  northwest  of  the  preceding. 

Maguire,  Kennedy  &  Co.  S.  E.  qr.  Sec.  28,  T.  7,  R.  1  E.  This  is  also  on  the  Dry- 
bone  Hollow  range.  The  shafts  here  are  from  sixty  to  seventy- five  feet  deep,  according 
to  the  surface  of  the  ground.  The  workings  are  in  the  Brown-rock  opening,  which  is 
here  about  eight  feet  high.  The  lead  ore  is  found  in  a  flat  sheet  in  the  bottom  of  the 
opening,  underlaid  by  pipe  clay. 

The  blende  was  discovered  in  the  spring  of  1874,  and  is  much  mixed  with  rock.  The 
ore  has.  to  be  crushed,  washed  and  separated.  Water  is  removed  from  the  diggings  by 
means  of  a  windmill  and  small  pump,  and  is  afterwards  utilized  to  wash  ore.  The  an- 
nual product  is  as  follows :  Lead  ore,  200  pounds ;  blende,  100  tons :  drybone  50  tons. 

Blackney,  Donahue  &  Co.  This  ground  is  owned  by  Dr.  Stanley  of  Highland,  and 
is  a  part  of  the  same  range  as  the  preceding,  and  situated  but  a  short  distance  north- 
east of  them.  The  range  here  makes  two  well-defined  openings  separated  by  a  cap- 
rock.  It  is  irregular  in  shape,  and  about  sixty  or  seventy  feet  wide,  with  little  water. 

The  following  is  a  section  of  their  principal  shaft. 

Feet. 

Galena  limestone 60 

First  opening    9 

Cap  rock ...    2 

Second  opening 4 

The  ore  is  found  in  flat  sheets,  and  is  Smithsonite,  blende,  and  lead,  the  former  being 
rather  impure.  The  present  parties  have  been  working  here  for  the  last  seven  years. 
The  annual  product  has  been  as  follows:  Lead  ore,  11,000  pounds;  Smithsonite,  35  tons; 
blende,  35  tons.  The  ground  here  seems  to  be  pretty  much  worked  out,  the  product 
being  chiefly  derived  from  the  old  workings. 


724  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

Speiusley  &  Co.  This  is  also  on  the  land  of  Dr.  Stanley,  and  is  a  short  distance  east 
of  the  preceding.  It  is  an  east  and  west  rang*,  situated  a  little  north  of  the  Dry  bone 
Hollow  range.  The  range  is  130  feet  wide,  so  far  as  has  been  worked,  and  may  prove 
to  be  200  feet  in  width  each  way  from  the  center.  The  ore  makes  in  pitches,  and  the 
sheet  varies  in  size  according  to  the  number  of  feeders  coming  in  from  above.  The  lead 
ore  occurs  much  mixed  with  rock,  which  necessitates  crushing  and  jigging  the  entire 
product. 

The  lot  worked  by  these  parties  consists  of  about  six  acres,  of  which  only  about  one- 
sixth  has  been  explored.  The  ore  is  blende  and  lead  ore;  some  Smithsom'te  is  said  to 
be  found  in  the  north  and  northwest  portions  of  the  ground,  while  the  blende  is  found 
in  the  southern  part.  The  amount  of  water  here  is  small,  and  is  all  removed  by  bail- 
ing, and  hoisting  in  a  barrel  containing  about  50  gallons. 

Three  shafts  have  have  been  sunk,  one  of  which  is  down  to  the  Blue  limestone,  and 
is  100  feet  deep 
The  company  have  operated  here  for  six  years,  with  the  following  product: 

Blende.  Lead  ore. 

Year.  tons.  Ibs. 

1871 70  60,000 

1872 150  120,000 

1873 350  150,000 

1874 250  160,000 

1875 300  257,000 

1876 325  300,000 


Siddel  &  Co.  They  are  situated  on  the  same  range,  worked  in  the  same  opening  as 
Spensley  &  Co.,  and  are  located  about  150  feet  east  of  them.  They  are  the  most  east- 
erly of  all  the  diggings  in  this  vicinity.  One  shaft  has  been  sunk,  and  the  ore  has  been 
found  to  make  in  the  same  manner  as  the  preceding,  except  that  this  ground  already 
furnishes  some  Smithsonite  from  the  north  side.  These  parties  have  been  working  here 
for  the  last  five  years,  during  which  time  the  average  annual  product  has  been  as  fol- 
lows: Lead  ore,  70,000  Ibs.;  Smithsonite,  85  tons;  blende,  70  tons. 

Flynn,  Lynch  &  Co.  On  Dr.  Stanley's  ground,  and  about  300  feet  southeast  of 
Spensley  &  Co.  Their  ground  is  a  lot  250  by  350  feet.  One  shaft  has  been  sunk  here 
80  feet  to  the  top  of  the  opening,  which  is  here  6  feet  high  and  100  feet  wide.  The 
ground  produces  lead  ore  and  blende,  occurring  in  a  flat  sheet,  mixed  with  the  top  layer 
of  the  Blue  limestone  and  some  pipe  clay.  The  company  has  been  working  about  five 
years,  since  which  time,  to  October,  1874,  they  have  produced  250,000  Ibs.  of  lead  ore 
and  700  tons  of  blende. 

Robinson's  Diggings.  Situated  about  300  feet  southeast  of  the  preceding,  on  the 
ground  of  Mr.  Barn«xd.  These  diggings  are  not  being  worked  at  present.  They  were 
commenced  in  the  winter  of  1871-2,  and  produced  4,500  Ibs.  of  lead  ore  and  about  9 
tons  of  blende  in  the  first  two  years. 

Williams  &  Edwards.  Situated  on  the  land  of  Mr.  Lampe  and  about  500  feet 
west  of  the  diggings  of  Blackney  &  Co.,  previously  described.  They  are  part  of  the 
Spensley  and  Lynch  range. 

The  works  are  in  the  Brown-rock,  which  here  appears  to  divide  into  three  subordinate 
openings.  A  section  of  their  working  shaft  is  as  follows,  all  in  the  Galena  limestone : 

Feet. 

Galena  limestone •  •  •  40 

First  opening 3 

Soft,  unproductive  ground 8 

Second  opening -.  •     3 

Soft,  unproductive  ground 8 

Third  opening  to  top  of  Blue  limestone S 


MINES— HIGHLAND  DISTRICT.  725 

These  diggings  consist  partly  of  old,  and  partly  of  new  workings.  Cross  cut  drifts 
are  run  through  the  old  works  in  search  of  new  ground,  lead  ore  being  usually  found  in 
the  lowest  opening.  These  parties  have  been  working  since  1870,  and  their  product  is 

as  follows : 

Lead  ore,       Smiihsonile, 

Tear.  Ibs.  torts. 

1870 70,000  70 

1871 70, 000  70 

1872 80,000  80 

1873 : 90,000  90 

1874 90,000  90 


The  production  of  the  years  1875  and  1876  was  net  ascertained. 

Harris  &  Stanley.     Situated  on  the  ground  of  Dr.  Stanley,  about  300  feet  north  of 
the  windmill  on  Kennedy  &  Co.'s  ground,  previously  described.    These  diggings  are 
quite  dry,  being  drained  by  the  windmill  pump.    The  range  appears  to  be  a  branch  of^ 
the  Drybone  Hollow  range,  about  500  feet  long,  running  in  a  north  and  south  direction. 
There  are  two  principal  openings  exhibited  in  the  following  section  of  their  working 

shaft: 

Feel, 

Galena  limestone 30 

First  opening ; 3 

Cap  rock  (limestone) 7 

Second  opening 6 

The  ore  occurs  as  usual  in  this  district,  in  flat  sheets.  These  parties  have  been  work- 
ing here  since  September.  1871,  since  which  time  to  October,  1874,  the  total  product  was 
as  follows:  lead  ore,  40,000  pounds;  blende,  35  tons;  Smithsonite,  75  tons. 

Rowe  &  Co.  Situated  on  the  N.  E.  qr.  of  Sec.  28,  T.  7,  R.  1  E,  comprising  160 
acres.  This  is  an  east  and  west  range,  known  as  the  Dunstan,  discovered  in  1846,  and 
worked  continuously  since.  It  is  about  half  a  mile  long,  and  200  feet  wide.  The  range 
is  worked  in  the  Brown-rock  opening,  chiefly  for  Smithsonite  and  lead  ore.  There  are 
three  working  shafts  from  50  to  75  feet  deep.  The  opening  is  from  5  to  20  feet  high. 
Their  annual  product  is  stated  at,  lead  ore,  50,000  Ibs.,  and  Smithsonite,  50  tons. 

This  was  all  that  could  be  elicited  relative  to  this  ground,  as  the  owners  were  quite 
reticent  on  the  subject. 

The  foregoing  comprise  all  the  diggings  in  the  imnu  diate  vicinity  of  Highland,  and, 
with  the  exception  of  the  last  (Rowe  &  Co.)  they  are  all  embraced  in  a  tract  of  land 
not  exceeding  forty  acres  in  extent.  The  same  general  geological  characteristics  pic- 
vail  in  all,  and  they  are  nearly  all  connected  together  in  the  workings.  The  ore  in  most 
of  them  has  to  be  crushed  and  jigged,  and  all  except  Kennedy  and  Maguire  have  to 
haul  their  wash  dirt  about  a  mile  and  a  quarter  to  water. 

In  these  diggings,  the  openings  below  the  top  of  the  Blue  limestone  have  never  been 
worked  or  even  prospected.  If  the  several  land-owners  would  take  some  concerted  ac- 
tion, a  level  might  be  run  up  the  Drybone  Hollow,  which  would  drain  them  to  any  depth 
required.  Such  a  work,  however,  should  be  preceded  by  boring,  to  ascertain  the  pres- 
ence of  flat  sheets  in  the  lower  openings,  the  existence  of  which  is  not  improbable. 

Mr.  Solomon  Spensley,  who  is  well  informed  on  the  subject,  says  that  the  annual  av- 
erage product  of  the  mines  is  approximately  as  follows:  Lead  ore,  1,000,000  Ibs.;  dry- 
bone,  1,350  tons;  blende,  1,200  tons.  In  addition  to  the  preceding,  there  are  some  dig- 
gings situated  south  of  the  village  of  Highland. 

Davis  &  Co.  Situated  near  the  S.  E.  cor.  of  Sec.  5,  T.  6,  R.  1  E.  This  is  a  north- 
west and  southeast  range,  discovered  by  a  Mr.  Styles  in  1862.  It  has  been  proved  to  a 


736     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

distance  of  450  feet,  with  an  average  width  of  40  feet.  The  opening  is  in  the  Brown 
rock,  and  from  four  to  six  feet  high.  There  are  two  shafts,  each  about  40  feet  deep. 
The  ore  occurs  in  flat  sheets,  and  is  mostly  Smithsonite  and  blende  in  about  equal  quan- 
tities, containing  little  lead  ore.  The  ground  was  formerly  worked  chiefly  for  blende. 

The  ground  is  estimated  to  have  produced  2,400  tons  of  blende,  and  1,100  tons  of 
Smithsonite  since  1862.  Their  present  annual  product  is  blende,  200  tons,  and  Sniith- 
sonite,  150  tons. 

Manning  &  Delaney.  Situated  about  600  feet  west  of  the  preceding.  It  is  an  east 
and  west  range  which  was  discovered  twenty  years  since,  and  has  been  worked  by  sev- 
eral different  parties,  who  have  proved  the  ground  in  the  Brown-rock  opening  for  a  dis- 
tance of  600  feet.  The  present  parties  have  worked  it  for  the  past  four  years,  princi- 
pally for  Smithsonite,  no  blende  being  found  until  the  spring  of  1874.  The  deepest 
shaft  is  only  40  feet;  sunk  to  the  top  of  the  Blue  limestone,  which  is  here  estimated  at 
25  feet.  The  St.  Peters  standstone  is  plainly  seen  in  the  valley  a  short  distance  below. 
The  ground  produced  600  tons  of  Smithsonite  during  the  years  1873  and  1874.  The 
diggings  are  quite  dry. 

Hornsnoggle  Ridge.  Situated  on  the  N.  E.  qr.  of  Sec.  5,  T.  6,  R.  1  E.  This  is  an 
east  and  west  range  about  half  a  mile  in  length,  which  was  discovered  about  twenty-five 
years  since,  and  worked  for  lead  ore  in  the  Brown-rock  opening;  but  is  now  pretty  much 
worked  out.  The  only  ore  found  on  the  ridge  is  drybone.  The  present  annual  produc- 
tion is  about  1,500  tons. 

Beginning  at  the  eastern  end,  and  going  west,  the  following  parties  are  working: 

Joseph  (/all.     Worked  here  since  1871,  amount  produced  unknown. 

Borey  &  Newmeyer.     Worked  since  1872,  produced  1,500  tons. 

Brinnen  &  Kelley.    Worked  on  a  lot  here  20  years,  product  1,000  tons. 

LINDEN  DISTRICT. 

The  principal  diggings  in  this  district  are  those  of  the  Linden  Mining  Co.,  owned  by 
Messrs.  J.  J.  Ross  and  Wni.  T.  Henry,  of  Mineral  Point.  The  property  consists  of  the 
E.  hf.  of  E.  hf.  of  Sec,  6,  W.  hf.  of  Sec.  5,  N.  E.  qr.  of  S.  W.  qr.  of  Sec.  7,  N.  E.  qr. 
of  S.  E.  qr.  of  Sec.  7,  S.  hf.  of  S.  W.  qr.  of  Sec.  8,  S.  W.  qr.  of  S.  E.  qr.  of  Sec.  8,  N. 
W.  qr.  of  N.  E.  qr.  of  Sec.  17,  S  hf.  of  N.  E.  qr.  of  Sec.  17,  all  in  T.  5,  R.  2  E.,  and  is 
situated  a  short  distance  west  of  the  village  of  Linden.  They  were  first  opened  in  1833, 
and  worked  by  various  parties  up  to  1853,  altogether  for  lead  ore,  and  in  the  middle 
beds  of  the  Galena  limestone.  Prior  to  1853,  they  are  said  to  have  produced  40,000,000 
K>s.  of  lead  ore. 

In  1853  they  were  bought  by  a  Pittsburg  company,  and  operated  with  a  water  wheel, 
in  the  upper  and  lower  pipe-clay  openings,  also  for  lead  ore.  The  amount  of  lead  ore 
produced  by  them  was  about  500,000  pounds  per  annum.  The  works  finally  became  un- 
profitable, and  were  suspended  by  them  in  1866.  In  this  condition  they  remained  until 
the  spring  of  1874,  when  they  were  bought  by  Messrs.  Ross  &  Henry,  by  whom  work 
was  resumed  in  April.  They  are  now  operated  for  blende  or  blackjack,  Smithsonite 
and  such  lead  ore  as  incidentally  occurs  with  it.  On  resuming  work  the  principal  ope- 
rations of  the  first  six  months  were  cleaning  out  the  old  shafts  and  drifts,  erecting  a  new 
engine  of  thirty  horse  power,  with  a  lift  pump,  together  with  the  necessary  buildings,  and 
other  machinery.  The  sheets  worked  here  have  a  singular  complication  of  "  flats  and 
pitches,"  both  in  their  connection  with  each  other,  and  in  respect  to  then- general  course, 
which  can  be  best  understood  by  reference  to  Plate  XXX.  The  lines  marked  North,  South, 
and  Middle  pitches,  are  inclined  and  flat  sheets,  consisting  chiefly  of  blende,  which  are  now 
being  worked.  The  shaded  portions  represent  the  ground  worked  out,  but  leaving  along 
the  sides  of  the  workings,  and  on  the  unworked  portions  of  the  several  pitches,  a  sheet  of 


PLATE.XXX 


MINES— LINDEN  DISTRICT.  727 

blende  mixed  with  lead  ore  and  associate  minerals,  of  from  one  to  three  feet  thick.  At- 
tention is  here  called  to  the  remarkable  curvature  of  the  sheets  or  pitches.  Beginning 
at  the  well  shaft,  they  take  a  northeasterly  course,  curving  around  to  a  northwesterly 
one  at  the  engine  shaft,  and  finally  to  a  westerly  one  at  the  west  pump  shaft.  But  one 
parallel  case  is  known  in  the  entire  Lead  region.  It  is  the  Watkins  range  of  the  Dodge- 
ville  district,  situated  in  the  same  opening,  and  worked'  for  the  same  ore. 

Although  the  blende  usually  occurs  in  a  large  sheet,  yet  it  is  frequently  connected 
with  two  or  three  parallel  smaller  ones  by  veins  or  "  pitches."  The  sheet  often  contains 
detached  pieces  of  the  wall  or  cap-rock,  of  various  sizes,  completely  surrounded  by  ore. 
Large  pockets  occur  in  the  bed,  lined  with  very  handsome  crystals  of  calcite,  one  of 
which,  recently  removed  from  the  mine,  measures  five  feet  by  two. 

Another  peculiarity  noticed  was  the  fin  ,ing  of  several  pieces  weighing  from  one  to 
five  pounds,  composed  of  wall-rock  and  ore,  which  were  rounded  and  worn  smooth,  re- 
sembling small  drift  bowlders.  They  were  found  in  the  lower  pipe-clay  opening,  and 
had  probably  been  detached  from  the  wall,  at  its  junction  with  the  ore.  They  must  have 
undergone  considerable  erosion  and  transportation,  or  movement,  by  subterranean  cur- 
rents of  water. 

The  workings  in  the  vicinity  of  the  eng'ne  shaft  were  first,  examined.  They  extend 
in  a  westerly  direction  a  distance  of  1,300  feet,  and  have  been  worked  to  a  width  of  45 
feet,  leaving  a  sheet  of  blende  on  the  northern  side  from  one  to  three  feet  thick.  It  has 
been  proved  by  a  cross  cut  to  connect  through  to  the  north  pitch,  a  distance  of  180  feet. 
The  same  sheet  has  been  worked  in  a  southerly  direction  nearly  to  the  well  shaft,  a  dis- 
tance of  600  feet,  leaving  a  large  sheet  of  blende  on  its  eastern  side.  These  workings 
are  in  the  glass- rock  opening,  and  about  twenty  feet  above  the  St.  Peters  sandstone. 

The  following  section  of  the  engine  shaft  will  explain  their  situation : 

Ft,        In. 

Dump  rock,  clay  and  soil 15 

Galena  limestone 72          6 

Blue  limestone 6         6 

Pipe  clay 1 

Glassrock   5 

Glass-rock  opening  (workings) 4 

Buff  limestone  to  bottom  of  shaft 8 

Buff  limestone  to  St.  Peters  sandstone 16 


Total 128        00 


The  workings  at  the  well  shaft  were  next  examined.  They  are  in  the  Brown-rock 
division  of  the  Galena  limestone,  and  about  26  feet  above  the  lower  workings.  As  will 
be  seen  on  reference  to  the  map,  the  ground  is  worked  in  an  irregular  shape  about  300 
feet  long,  by  150  feet  wide 

It  is  estimated  that  $200,000  worth  of  ore  has  been  taken,  in  the  course  of  all  opera- 
tions, from  this  small,  irregular  piece  of  ground.  It  was  full  of  large  flat  sheets  and 
pitches,  and  was  worked  in  some  places  to  a  height  of  20  feet.  It  now  produces  30  tons 
of  zinc  ore  per  week,  and  considerable  lead  ore.  This  is  exclusive  of  the  ore  raised  by 
numerous  miners  working  here  on  tribute. 

Fig.  19  illustrates  the  manner  in  which  the  flat  and  pitching  sheets  are  connected  in 
the  ground.  It  is  taken  from  a  point  on  the  south  pitch,  northeast  of  the  well  shaft. 

Two  sheets  were  observed.  One,  A,  coming  down  through  the  drift.,  aaid  pitching  to 
the  south,  and  the  other  coming  in  from  the  north  en  a  flat  E,  making  a  pitch  to  D, 
a  second  at  flat  C,  and  a  second  pitch  at  B,  through  the  floor  of  the  drift.  At  B  it  is  only 
about  three  feet  distant  from  the  sheet  A.  It  is  known  from  the  extension  of  the 


728  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


connected  with  the  engine  shaft  that  the  two  unite  below  and  make  a  large  sheet  (as  is 
usually  the  case),  which  continues  down  to  the  lower  opening. 

At  the  west  pump  shaft 

a  winze1  was  sunk  by  a  FIG.  19. 

former  company  to  a 
depth  of  40  feet  in  the 
St.  Peters  sandstone,  with 
the  intention  of  penetrat- 
ing through  the  forma- 
tion. A  small  amount  of 
blende  is  said  to  have 
been  found,  but  no  regu- 
lar sheet.  Considerable 
ferruginous  matter  was 
also  found. 

There  appears  to  be  no 
reason  why  the  ground 
should  not  continue  remunerative  for  a  long  time,  as  it  is  comparatively  easy  to  work, 
and  the  amount  of  water  relatively  small.  It  seems  quite  likely  that  these  ranges  may 
connect  on  the  north  with  Morrison's  diggings,  p.  729,  and  on  the  south  with  the  Faul  dig- 
gings, p.  729;  should  the  latter  prove  true  the  mines  would  all  drain  into  the  creek  near 
Linden,  and  be  worked  at  much  less  expense. 

It  is  estimated  by  the  owners  that  during  the  first  six  months  of  their  operation,  the 
mine  produced  ten  tons  of  zinc  ores  per  day;  and  from  that  time  to  the  present  it  has 
produced  twenty  tons  of  zinc  per  day,  and  more  than  300,000  pounds  of  lead  ore  per 
annum.  The  value  of  all  ores  for  the  last  two  years  is  estimated  at  $500  per  day.  The 
mine  now  furnishes  constant  employment  to  one  hundred  and  eighty  miners  and  other 
employes.  The  owners  have  lately  introduced  the  Ingersoll  pneumatic  drill  with  air 
compressor;  and  use  Rend  rock  extensively,  the  explosions  b3ing  effected  by  an  electric 
battery. 

Poad,  Barrett  &  Tredinnick  Bros.    S.  W.  qr.  of  N.  W.  qr.,  Sec.  8,  T.  5,  R.  2  E. 

This  is  a  very  old  mine,  the  property  of  Mr.  John 
Heathcock,    known    as    tl  e    Robarts  mine,   on 
which  work  had  been  discontinued  for  several 
/  years,  until  1869,  when  it  was  again  resumed. 
The  present  party  have  been  working  about  four 
2  years,  and  have  sunk  ten  shafts  from  40  to  70  feet 
deep.    The  water  is  removed  by  two  horse  pumps. 
To  the  west  of  the  above  parties,  and  on  the  same 
j  range,  are  Kisselbury  Bros.,  Hammersoa  and 
2  Trewatha.     Also  on  the  east  end  of  the  same 
range  are  the  Poad  Bros.,  Tredinnick,  Vial 
1  and  Geach. 

The  Robarts  range  has  been  traced  for  a  dis- 
tance of  a  quarter  of  a  mile,  the  ore  being  found 
in  flat  sheets,  25  feet  above  the  glass  rock.    The 
manner  in  which  the  ore  is  deposited  is  very  re- 
markable, and  is  shown  in  the  annexed  sketch, 
from  which  it  appears  that  fie  order  of  deposition 
was,  1st,  pyrites;  2d,  blende;  -V,  galenite.    This 
is  one  of  the  few  localities  in  the  Lead  region  from  which  cerussite  is  ou  ained.' 
1  A  winze  is  a  subterranean  shaft  which  does  not  extend  to  the  surface. 


FIG.  20. 


SECTION  OF  SHEETS  IN  THE  POAD  MINE. 

1.  Galena  limestone,  cap  and  floor  of 
opening.  2.  Sheet  of  Iron  Pyrites  3  to 
4  inches  thick.  8.  Sheet  of  Blende  1  in. 
thick.  4.  Sheet  of  Galenite  1  to  6  inches 
thick. 


MINES  — LINDEN  DISTRICT.  729 

The  three  mines  on  the  Robart's  range  are  estimated  to  produce  annually  200,000 
pounds  of  lead  ore,  and  100  tons  of  blende. 

Treglown  &  Sons  and  Capt.  Wicks.  S.  W.  qr.  of  N.  W.  qr.  Sec.  8,  on  the  west 
side  of  the  Heathcock  branch.  Wearing  &  Golclsworthy,  owners.  This  range  was  dis- 
covered about  forty  years  ago,  and  has  been  worked  continuously  ever  since.  The  present 
company  have  been  working  it  during  the  last  two  years  in  the  glass-rock  opening. 
The  ore  is  found  about  fifteen  feet  below  the  surface;  the  width  of  the  range  is  45 
feet,  drained  by  a  level  40  rods  long.  In  former  years  it  was  worked  for  Smithsonite  at 
higher  levels,  and  was  quite  productive.  Its  present  annual  production  is,  lead  ore, 
5,000  pounds;  blende,  100  tons. 

Adams  &  Son  and  JBowden.  These  parties  are  situated  about  a  quarter  of  a  mile 
southwest  of  Treglown  &  Wicks.  They  have  been  working  during  the  last  seven 
years  on  the  Morrison  range,  producing  annually  about  50  tons  of  Smithsonite,  and 
7,000  pounds  of  lead  ore.  Water  was  removed  from  these  diggings  by  drilling  a  hole 
down  to  the  glass-rock  opening. 

David  Morrison  Diggings.  W.  hf .  of  S.  W.  qr.  Sec.  8.  The  range  is  about  700 
yards  long,  40  feet  wide,  and  has  a  general  north  and  south  course.  The  range  was 
discovered  in  1846,  and  worked  at  various  times  for  lead  ore  to  1874.  Mr.  Morrison 
then  opened  the  main  sheet  of  blende,  since  which  time  the  production  has  been  as  fol- 
lows: in  1874,  90  tons;  in  1875,  106  tons.  During  the  present  year  the  mine  has  not 
been  worked,  although  it  is  still  good.  The  range  is  drained  by  a  level  350  feet  long. 
The  ore  is  found  in  flat  sheets  from  7  to  10  inches  thick,  on  the  top  of  the  glass  rock. 

Richards  &  Faul  Bros.  These  diggings  are  situated  in  the  village  of  Linden,  near 
the  S.  E.  corner  of  section  8,  on  land  owned  by  Wm.  George.  The  ore  is  found  under 
the  glass  rock  in  a  flat  sheet  from  10  to  1%  inches  thick,  from  15  to  25  feet  in  width,  and 
from  13  to  30  feet  below  the  surface.  The  water  is  removed  by  a  drain  about  150  feet 
long.  This  mine  was  discovered  in  May,  1875.  From  that  time  to  May,  1876,  they 
produced  80,000  Its.  of  lead  ore,  and  150  tons  of  blende.  During  July,  August  and 
September,  1876,  they  have  produced  35,000  flbs.  of  lead  ore,  and  40  tons  of  blende. 

Thomas  Tamblin.  Zinc  ores  were  discovered  on  the  N.  W.  qr.  of  the  N.  W.  qr  of 
Sec.  10,  T.  5,  R.  2  E.,  on  the  20th  of  December,  1875,  on  the  land  of  Mrs.  Thos.  Shore. 
The  general  course  of  the  range  is  nearly  east  and  west,  and  is  now  worked  at  an  average 
depth  of  10  feet  below  the  .surface,  and  has  been  proved  to  a  distance  of  40  feet.  The 
ore  was  found  as  a  flat  sheet  of  drybone,  cropping  out  at  the  foot  of  a  hill;  on  working 
into  the  hill  the  amount  of  Smithsonite  was  found  to  diminish,  and  the  blende  to  in- 
crease; which  seems  to  be  an  indication  that  the  Smithsonite  is  a  secondary  product, 
derived  from  the  blende.  It  is  estimated  that  two  miners  can  produce  here  100  tons  of 
zinc  ore  per  annum. 

R.  S.  &  W.  J.  Jacobs.  S.  E.  qr.  of  S.  W.  qr.,  and  S.  W.  qr  of  S.  E.  qr.  section 
7,  T.  5,  R.  2  E.  This  mine  was  discovered  in  March,  1875.  There  are  here  four  east 
and  west  sheets,  from  four  to  six  feet  wide  and  from  four  to  six  inches  thick  in  the  upper 
pipe-clay  opening,  separated  from  each  other  by  six  or  eight  feet  of  unproductive  rock. 
They  are  worked  about  20  feet  below  the  surface.  There  is  but  a  small  amount  of 
water,  which  is  bailed  out.  Some  very  large  isolated  masses  of  lead  ore  have,  been 
found  here,  one  of  which,  weighing  1,527  H>s.,  was  sent  to  the  Centennial  Exhibition. 
Small  quantities  of  zinc  ores  are  also  found.  The  mine  produced  during  the  year  1875, 
of  lead  ore,  70,000  ft>s.,  and  in  1876,  40,000  flbs.  The  mine  has  not  been  worked  much 
during  this  summer,  as  the  owners  are  engaged  in  farming. 


730 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


DODGEVILLE  DISTRICT. 

The  mines  of  this  district  comprise  those  in  the  immediate  vicinity  of  the  village;  the 
zinc  ore  diggings  situated  about  two  miles  east  of  the  village,  and  those  on  Van  Meter's 
survey,  about  four  miles  west  of  the  town. 

The  most  productive  and  profitable  are  those  situated  east  of  the  village,  worked  for 
drybone,  blende  and  lead  ore. 

Evan  Williams'  Mines.  S.  W.  qr.  of  S.  W.  qr.  Sec.  25,  T.  6,  R.  3  E.  These  mines 
were  discovered  in  1844,  and  were  worked  at  intervals  until  1853.  Since  then  Mr.  Wil- 
liams has  worked  them  continuously  to  date.  The  ore  is  found  in  flat  sheets  about  100 
feet  wide  in  the  lower  beds  of  the  Galena  limestone;  and  the  ground  is  drained  by  a 
level  a  quarter  of  a  mile  long.  The  annexed  sketch,  made  from  an  underground  sur- 
vey, shows  some  of  the  more  recent  works. 

FIG.  21. 


PLAN  OF  EYAN  WILLIAMS'  DIGGINGS. 


Mr.  Williams  estimates  that  this  range  has  averaged  50,000  pounds  of  lead  ore  per 
annum  during  the  last  twenty  years.  Previous  to  1863,  they  were  worked  exclusively 
for  lead  Ore.  Since  then  they  have  averaged  100  tons  per  annum  of  blende;  the  pro- 
duction rising  in  some  years  to  200  tons.  During  the  present  year  (1876)  two  men  have 
been  employed  here,  and  have  produced  30,000  pounds  of  lead  ore  and  125  tons  of 
blende. 

In  November,  1875,  Mr.  Williams  commenced  working  about  700  feet  south  of  the 
preceding  location.  A  flat  sheet  was  found  here  at  a  depth  of  90  feet,  and  has  been 
proved  horizontally  a  distance  of  60  feet.  This  mine  in  the  past  year  has  produced,  lead 
ore  15,000  pounds;  blende,  50  tons. 

In  July,  1876,  Mr.  Williams  sunk  a  shaft  25  feet  deep  about  quarter  of  a  mile  west  of 
the  center  of  Sec.  25,  and  discovered  aflat  sheet  of  blende  about  five  inches  thick,  from 
which  he  has  obtained  about  three  tons  of  blende. 

Owens  &  Powell.  On  the  S.  W.  qr.  of  S.  E.  qr.  of  Sec.  25  are  some  small  drybone 
diggings  on  Mr.  Williams'  land.  Three  men  are  employed  here,  producing  five  tons  of 
ore  per  annum.  This  is  known  as  Rounds'  range. 

Jones,  Farrager  &  Owens.  S.  W.  qr.  of  S.  W.  qr.  of  Sec.  25,  near  the  west  line 
of  the  section  on  Evan  Williams'  land.  This  is  an  old  range  which  has  been  worked 


PL  ATE,  XXII 


MINES  —  DODGE VILLE  DISTRICT.  731 

since  its  discovery  in  1849.  The  range  is  drained  by  a  level  300  yards  long.  The  ore  is 
found  in  Hat  sheets,  from  45  to  SO  feet  below  the  surface.  Five  shafts  are  now  open. 
These  diggings  produce  only  lead  ore.  The  annual  product  is  valued  at  from  $3,000  to 
$5,000. 

Mrddth  Evans.  X.  E.  qr.  of  X.  W.  qr.  Sec.  25,  on  John  Williams'  land.  These 
diggings  are  on  Morgan  Jones'  old  range,  and  have  been  worked  during  the  last  four 
years  for  Smithsonite.  During  the  present  year  (1876)  lead  ore  and  blende  have  been 
discovered,  and  65,000  pounds  of  lead  ore  have  been  produced  and  considerable  blende. 

Hugh  Jones.  N.  E.  qr.  of  1ST.  W.  qr.  Sec.  25.  These  diggings  are  on  the  eastern 
portion  of  the  Watkins  range.  They  were  discovered  in  1848.  The  present  party  com- 
menced work  in  1864.  The  ore  is  found  in  an  irregular  flat  sheet,  from  100  to  200  feet 
wide,  in  the  lower  part  of  the  Galena  limestone.  Its  position  will  be  best  understood 
by  reference  to  the  diagram  of  the  Watkins  range .  The  annual  product  of  this 
mine  is,  lead  ore,  25,000  pounds,  blende,  150  tons. 

Hendy,  Davey,  Sobey  &  Co.  N.  W.  qr.  of  N.  W.  qr.  Sec.  36,  T.  6,  R.  3  E. 
These  diggings  comprise  the  southern  and  western  portions  of  the  Watkins  range.. 
Their  position  is  explained  on  the  annexed  map. 

Several  persons  have  been  engaged  in  mining  here  for  a  number  of  years.  The  ore 
is  blende  and  lead  ore,  found  in  a  flat  sheet  in  the  same  opening  and  position  as  in  the 
Hugh  Jones  diggings.  The  works  extend  eastward  and  will  ultimately  connect  with 
them,  the  intervening  space  being  about  100  feet.  The  mine  has  been  and  is  now  quite 
productive,  the  exact  amount  could  not  be  ascertained. 

Samuel  Clegg.  N.  E.  qr.  of  S.  E.  qr.  Sec.  26,  T.  6,  R.  3  E.  The  land  is  owned 
by  Mr.  A.  P.  Thompson,  of  Buffalo.  The  ore  is  found  in  a  flat  sheet  in  the  glass-rock 
opening,  and  is  obtained  from  three  shafts,  each  100  feet  deep.  Lead  ore  only  is  pro- 
duced; it  was  discovered  in  1870,  and  produced  in  that  year  20,000  pounds.  Since  that 
time  to  October  1, 1876  the  total  product  has  been  600,000  pounds. 

VVm.  Carter  &  Owens.  W.  hf .  of  S.  E.  qr.  Sec.  26.  Owner  of  land,  A.  P.  Thomp- 
son of  Buffalo.  This  is  known  as  Edward  Edwards'  range,  and  was  discovered  in  1853. 
The  range  has  a  general  north  and  south  course,  but  with  some  irregularities.  It  was 
worked  north  500  feet,  then  west  600  feet,  then  north;  the  north  and  south  portions 
being  the  most  productive  of  lead  ore.  The  mine  is  quite  wet,  but  is  drained  by  a  level 
about  2,000  feet  long.  The  number  of  shafts  is  nine,  the  greatest  depth  below  the  sur- 
face being  70  feet.  The  length  of  the  drift  is  1,250  feet.  Mr.  Carter  has  been  working 
this  mine  for  six  years.  During  that  time  the  product  of  the  east  and  west  portion  has 
been  65,000  pounds  of  lead  ore  annually,  and  in  the  north  and  south  portions  150,000 
pounds  per  annum,  with  the  same  expense. 

Other  parties  working  in  this  vicinity  are  Nicholas  Bailey  &  Co.  and  John  Bosan- 
co  &  Co. 

Joseph  Pearce  Diggings.  This  mine  is  situated  in  the  village  of  Dodgeville,  a 
short  distance  northwest  of  the  court  house.  It  is  known  as  the  Lowry  range,  and  was 
discovered  in  1836.  It  was  not  worked  from  1850  to  1870,  when  Mr.  Pearce  commenced 
work  on  it,  and  has  worked  it  continuously  ever  since.  It  is  worked  exclusively  for  lead 
ore,  which  is  found  in  tumbling  openings  and  in  flat  sheets  from  50  to  70  feet  wide. 
The  range  is  drained  by  a  level  800  feet  long  to  a  depth  of  30  feet  below  the  surface. 
The  deepest  shaft  is  80  feet. 

There  is  considerable  water  in  the  mines,  but  much  less  than  there  was  25  years  since. 
The  water  is  removed  by  a  horse  pump  worked  during  the  daytime.  The  length  of  the 
range,  so  far  as  it  has  been  worked,  is  1,000  feet.  During  tile  last  two  years  this  mine 
has  produced  200,000  pounds  of  lead  ore;  previous  to  this  it  only  paid  expenses. 

Lainbly  Range.  N.  E.  qr.  Sec.  28,  T.  6,  R.  3  E.  This  range  has  been  worked  con- 
tinuously for  a  great  many  years,  and  now  gives  employment  to  four  men.  It  pro- 


732  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

duces  lead  ore  to  the  amount  of  about  30,000  pounds  per  annum.    Four  years  ago  its 
annual  product  was  200,000  pounds. 

Porter's  Grove  Diggings. 

These  mines  are  situated  in  town  6,  range  4  east.  At  present  the  following  mines  are 
in  operation: 

Union  Mine,  AVm.  Hendy  &  Co.  Situated  on  the  N.  E.  qr.  of  the  N.  E.  qr.  of  Sec. 
28.  The  ore  produced  is  lead,  and  in  tumbling  openings,  at  a  depth  of  70  feet  and  on 
the  upper  surface  of  the  green  rock.  From  two  to  five  men  are  employed.  The  min  e 
is  drained  by  a  level  one-quarter  of  a  mile  long. 

Ridgeway  Mine,  Win.  Hendy  &  Co.  Situated  on  the  S.  E.  qr.  of  the  S.  E.  qr.  of 
Sec.  21.  This  mine  is  owned  and  operated  by  the  same  parties  as  the  preceding,  and 
is  on  the  same  range,  which  is  known  as  the  north  and  south  branch  lot.  From  two  to 
four  men  are  employed.  It  is  also  drained  by  a  level  a  quarter  of  a  mile  long.  The 
mode  of  occurrence  of  the  ore  is  also  the  same.  The  present  owners  commenced  opera- 
ting them  in  1872;  since  then  the  product  of  lead  ore  is  as  follows: 

Union  Ridgrway 

Mine.  Mine. 

1872 300,000  fts.    44,000  &s. 

1873 35,000  "  44,000  " 

1874 16,000  "  63,000  " 

1875 38,000  "  44,000  " 

1876  to  Oct.  1st , 22,000  "  17,000  " 


Frank,  Farwell  &  Co.  S.  E.  qr.  of  N.  E.  qr.  of  Sec.  28.  These  parties  commenced 
working  on  the  Wakefield  range  in  Oct.,  1875.  Previous  to  that  time  it  had  not  been 
worked  for  twenty  years.  Most  of  the  workings  are  at  a  depth  of  35  feet  below  the  sur- 
face, although  some  are  as  deep  as  60  feet.  The  work  is  chiefly  removing  pillars  of  lead 
ore  -which  have  been  left  from  former  operations.  The  product  from  Oct.,  1875,  to  Oct., 
1876,  has  been  14,000  Bbs. 

Other  parties  mining  in  this  vicinity  are  John  and  Thomas  Paull,  of  Ridgeway,  pro- 
ducing lead  ore. 

Van  Meter's  Survey. 

On  the  N.  hf.  of  the  N.  E.  qr.  of  Sec.  18,  T.  5,  R.  3  E.,  are  three  very  large  ranges 
•which  have  not  to  our  knowledge  been  reported.  Their  general  course  is  N.  W.  and  S. 
E.,  and  they  are  crossed  by  numerous  north  and  south  crevices.  It  is  at  these  cross-ings 
that  the  largest  bodies  of  ore  are  found.  The  ore  is  galenite,  and  is  entirely  free  from 
any  mixture  of  zinc  ores.  It  is  found  in  the  green-rock  opening. 

The  northernmost  of  the  three  ranges,  known  as  the  Duke  Smith,  contained  an  open- 
ing in  places  50  feet  wide,  somewhat  intersected  with  bars.  It  was  worked  over  a  quar- 
ter of  a  mile  in  length,  and  produced  about  half  a  million  pounds  of  lead  ore.  It  has 
not  been  worked  since  1853. 

A  short  distance  south  of  this  is  a  parallel  range  which  produced  over  200yOOO  ft>s.  in 
a  distance  of  about  100  feet.  The  opening  was  about  30  feet  wide. 

The  third  parallel  range,  300  feet  south  of  the  Duke  Smith  range,  has  been  worked 
since  the  winter  of  1873-4,  by  Mr.  John  Hutchinson  of  Mineral  Point.  The  lead  ore 
occurs  in  large  pockets  containing  crystalline  pieces  of  from  one  to  five  hundred  pounds 
weight.  The  opening  is  in  the  green  rock  and  is  from  ten  to  twelve  feet  high.  This 
range  has  been  the  least  worked  of  all,  but  formerly  produced  about  100,000  pounds. 
It  now  yields  ore  of  the  value  of  $5  per  day  when  worked.  None  of  the  ranges  have  been 
worked  to  any  great  depth,  and  all  were  abandoned  with  ore  going  down  in  the  cre- 
vices. The  gradual  diminution  of  water  in  the  country  has  now  made  it  possible  to  re- 
sume work. 


MINES  — MINERAL  POINT  DISTRICT.  733 

Powell  &  Co.  This  party  is  working  on  what  is  known  as  the  Nic  Schillen  range. 
Work  was  commenced  in  the  spring  of  1876,  and  continued  for  three  months.  The 
works  are  in  the  glass-rock  opening  and  about  20  feet  below  the  surface.  The  amount 
produced  was  3,000  pounds. 

Richards  &  Burns.  This  party  is  situated  south  of  the  preceding,  and  on  land  of 
the  Sterling  estate.  They  have  been  working  these  during  the  present  year  in  the 
green-rock  opening,  producing  about  2,000  pounds  per  month. 

Powell  Diggings.  They  are  situated  about  a  quarter  of  a  mile  north  of  Mr. 
Hutchinson's  diggings.  This  is  a  new  discovery  and  has  been  in  operation  about  a  year. 
The  production  has  been  35,000  pounds. 

3IINERAL  POINT  DISTRICT. 

These  mines  comprise  those  in  the  immediate  vicinity  of  the  city,  and  those  of  Lost 
Grove  and  Diamond  Grove.  Considerable  mining  is  being  carried  on  at  these  localities, 
which  are  among  the  oldest  and  most  productive  of  the  Lead  region.  They  are  all  com- 
prised in  towns  4  and  5,  ranges  2  and  3  east.  In  addition  to  the  lead  ore,  a  great  deal 
of  zinc  ore  has  been  produced  within  the  past  ten  years,  and  they  now  supply  a  large 
portion  of  the  zinc  ore  of  the  Lead  region. 

Terrill  Range  and  Badger  Range.  These  ranges  are  situated  on  lots  128,  129, 
130,  131,  132,  134  of  Harrison's  survey  of  the  city  of  Mineral  Point.  They  are  old  and 
well  known  ranges,  which  have  been  worked  continuously  for  many  years,  and  are  now 
productive  of  Smithsonite  and  galenite.  They  furnish  constant  employment  to  about 
twenty-five  men. 

The  mines  are  situated  on  a  high  ridge,  from  which  the  water  drains  naturally  into 
the  adjacent  ravines,  leaving  the  diggings  constantly  dry.  The  ore  is  found  in  flat 
sheets  and  "pitches"  (inclined  sheets).  The  ranges  are  from  150  to  200  feet  wide, 
more  than  a  quarter  of  a  mile  long,  and  contain  ore  at  depths  varying  from  10  to  60 
feet  below  the  surface.  There  are  three  principal  openings  in  the  lower  beds  of  the  Ga- 
lena limestone.  The  parties  now  working  on  the  Terrill  range  are  as  follows: 

Matt  Shields  and  John  Linden.  They  have  been  working  for  three  years,  at  an 
average  depth  of  40  feet,  producing  chiefly  Smithsonite  from  the  second  opening.  The 
sheet  averages  about  ten  inches  in  thickness. 

Pascoe  &  Collins.  They  have  been  working  their  present  mine  during  the  last 
eight  years,  producing  Smithsonite,  blende  and  galenite  from  the  green  rock  and  the 
green-rock  opening.  The  Smithsonite  is  the  most  abundant,  and  the  lead  ore  the  least 
so.  The  workings  are  from  20  to  60  feet  deep,  and  the  ore  is  found  in  sheets  from,  one 
to  four  inches  thick.  The  blende  is  found  at  the  greatest  depth,  and  averages  about 
four  inches  in  thickness. 

Jacka  &  Waggoner.  These  parties  have  been  working  here  eight  years,  at  a  depth 
of  about  50  feet  below  the  surface,  but  never  having  reached  the  lower  opening.  They 
estimate  their  annual  production  at  15,000  Ibs.  of  galenite  and  25  tons  of  Smithsonite. 
The  range  at  this  point  is  200  feet  wide. 

Hitchins  &  Terrill.  They  have  been  working  at  various  times  during  the  last  ten 
years  on  the  northwest  end  of  the  Terrill  range,  known  as  the  brush  lot,  producing  lead 
and  zinc  ore.  This  was  formerly  very  rich  ground.  The  work  at  present  is  confined  to 
prospecting. 

Huxtable  &  Son.  These  parties  are  working  near  the  center  of  the  range,  and  from 
20  to  50  feet  deep,  producing  large  amounts  of  lead  and  zinc  ore.  This  is  believed  to 
be  one  of  the  best  mines  on  the  range. 

Parties  working  on  the  Badger  range  are  as  follows : 

Thos.  Cox  &  Sons.    These  parties  are  working  near  the  center  of  the  range,  and 


734     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

have  been  mining  here  during  the  last  ten  years.  The  ore  is  found  in  three  flat  open- 
ings. The  first  is  from  ten  to  twenty  feet  below  the  surface,  and  contains  chiefly  Smith  - 
sonite  in  sheets  of  three  inches  thickness.  The  second  opening  is  ten  feet  deeper,  con- 
taining the  same  ore,  mixed  with  galenite,  in  sheets  of  three  inches.  The  third  open- 
ing is  ten  feet  below  the-  second,  and  contains  chiefly  blende  in  sheets  averaging  four 
inches.  The  description  of  these  openings  applies  to  all  the  other  mines  in  the  range. 

Other  parties  working  on  this  range  are  Cox  &  Co.,  Jas.  Hitching  &  Holinan,  and 
Harris  and  partner. 

The  mining  ground  on  this  ridge  is  owned  in  small  lots  by  several  parties,  among 
whom  are  Messrs.  Ross,  Priestly,  Tyck  and  Prideaux.  [t  was  found  impossible  to  ob- 
tain any  information  of  the  amounts  of  ore  produced  on  this  ridge,  but  it  is  safe  to  esti- 
mate ore  to  the  amount  of  $600  per  annum  for  each  man,  and  this  is  probably  much 
beneath  the  actual  amount. 

William  Prideaux  Mines.  S.  E.  qr.  of  N.  W.  qr.,  Sec.  30,  T.  5,  R.  3  E.  This  is  a 
part  of  the  Ashbank  range,  so  called  from  the  decomposed  appearance  of  much  of  the 
surface  lead  ore.  It  was  discovered  more  than  thirty  years  since,  and  worked  er- 
tensively  for  lead  ore.  The  course  of  the  range  is  nearly  northwest,  and  its  average 
width  about  25  feet.  The  principal  product  of  the  mine  is  Smithsonite,  with  some  lead 
ore.  The  workings  are  chiefly  in  the  green-rock  opening,  where  the  ores  are  found  in 
flat  and  pitching  sheets,  from  two  to  eighteen  inches  thick.  The  ground  is  dry  and  the 
workings  rather  shallow,  seldom  being  more  than  fifty  feet  below  the  surface.  In  one 
place,  where  water  was  troublesome,  it  was  removed  by  drilling  a  hole  54  feet  deep, 
draining  it  off  through  a  lower  opening.  During  the  present  year  (1876).  about  51,000 
pounds  of  lead  ore  and  some  blende  were  obtained  in  the  Brown-rock  opening.  Mr. 
Prideaux  commenced  work  in  April,  1873,  and  now  employs  six  men.  He  estimates 
that  from  January  1,  to  October  1,  1876,  the  value  of  ores  produced  is  $6,500,  and 
about  the  same  amount  from  April,  1873,  to  January  1,  1876. 

A  short  distance  southwest  of  the  preceding,  is  a  parallel  range  not  worked  at  present, 
but  regarded  as  a  valuable  mining  ground. 

J.  Jackson  &  Co.  These  diggings  are  also  on  the  Ashbank  range,  and  a  short  dis- 
tance east-of  Wm.  Prideaux.  The  ores  produced  are  Smithsonite  and  galenite  in  nearly 
equal  amounts,  found  in  flat  sheets  in  the  green  rock,  and  its  opening  from  15  to  40  feet 
below  the  surface.  The  range  is  about  40  rods  long  and  350  feet  wide ;  ten  shafts  have 
been  sunk  upon  it.  Work  was  commenced  here  in  1868,  since  which  time  it  has  been 
continuous,  the  mines  proving  very  productive.  No  exact  amounts  could  be  ascertained, 
but  the  owners  estimate  the  value  of  ores  produced  since  1868  at  $18,000;  the  present 
year  being  the  most  remunerative. 

Mitchell  &  Pollard.  N.  W.  qr,  of  S.  W.  qr.  Sec.  30,  T.  5,  R.  3  E.  This  range  is 
situated  about  60  rods  southwesterly  from  the  Prideaux  mines.  These  parties  have  been 
working  about  four  years,  producing  Smithsonite  and  lead  ore.  The  workings  are  shal- 
low and  dry,  similar  to  the  Ashbank  range,  but  not  so  productive. 

Sinapee  Diggings.  These  mines  are  situated  on  the  N.  E.  qr.  of  S.  E.  qr.  of  Sec. 
30.  They  were  discovered  in  1845,  have  been  worked  continuously  since  then,  and  now 
furnish  employment  to  several  parties,  among  whom  are: 

Samuel  Prisk  and  Win.  Paynter.  These  parties  commenced  work  in  the  fall  of 
1875,  and  have  produced  during  the  last  year  about  50  tons  of  Smithsonite  and  some 
lead  ore.  The  diggings  are  quite  diy  and  average  about  15  feet  in  depth.  The  ore  is 
found  in  flat  sheets  the  principal  workings  being  in  the  glass -rock  opening.  Four  men 
are  employed  here.  This  mine  furnishes  fine  cabinet  specimens  of  galenite.  The  range 
is  about  500  feet  long,  from  100  to  150  feet  wide,  and  has  a  general  east  and  west 
course.  The  ore  sheet  is  from  two  to  four  inches  thick. 

Prisk  &  Coad.    This  is  a  parallel  range  situated  about  300  feet  south  of  the  preced- 


MINES  — MINERAL  POINT  DISTRICT.  735 

ing,  and  having  about  the  same  length,  width  and  thickness.  The  above  party  com- 
menced work  in  the  fall  of  1875,  and  are  now  working  in  the  upper  pipe-clay  opening. 
This  mine  is  from  50  to  60  feet  deep,  and  formerly  produced  over  a  million  pounds. 
Two  men  are  generally  employed  here,  and  produced  during  the  last  year  about  7,000 
pounds  of  lead  ore. 

Samuel  ami  Wm.  Richards.  These  parties  are  working  a  short  distance  east  of  Prisk 
&  Paynter.  They  have  been  engaged  here  about  a  year  and  a  half,  producing  chiefly 
blende  and  lead  ore. 

Bennett  &  Brady.  Situated  near  the  center  of  Sec.  29.  A  large  amount  of  work 
has  been  done  here,  including  a  level  to  unwater  the  ground.  They  are  quite  product- 
ive of  the  ores  of  zinc  and  lead. 

Short  &  Co.  Situated  on  the  N.  W.  qr.  of  Sec.  29.  Considerable  mining  has  been 
done  by  these  parties  in  this  vicinity  during  the  last  few  years. 

There  are  several  very  profitable  mines  in  the  northwestern  part  of  Strong's  Addition 
to  the  city  of  Mineral  Point,  all  on  land  owned  by  Mr.  J.  J.  Ross.  They  are  as  follows: 

Bohan  &  Co.  Four  men  have  been  employed  here  during  the  last  four  years,  pro- 
ducing Smithsonite  and  lead  ore.  The  range  is  from  70  to  80  feet  wide,  has  a  general 
east  and  west  course,  and  is  worked  to  a  depth  of  70  feet  below  the  surface.  There  are 
two  openings,  separated  by  about  20  feet  of  unproductive  rock;  the  lower  ore  being 
the  glass-rock  opening. 

Connanghton  &  Casserly.  These  parties  are  working  on  an  east  and  west  range 
about  300  feet  north  of  the  preceding.  They  have  been  working  here  during  the 
last  two  years,  have  sunk  two  principal  shafts  to  a  depth  of  60  feet,  to  the  glass-rock 
opening.  This  is  an  east  and  west  range,  about  60  feet  wide,  and  has  been  drifted  on 
to  a  distance  of  100  feet.  It  produces  chiefly  blende,  estimated  by  the  owners  at  $800 
per  year. 

John  \Vcegler  &  Co.  Situated  about  300  feet  northwest  of  the  preceding.  These 
parties  are  working  in  the  same  openings  and  producing  chiefly  zinc  ores.  Until  very 
recently,  two  other  parties  were  employed  in  this  vicinity,  this  ridge  having  for  many 
years  been  very  good  mining  ground. 

Bennett  &  Co.  This  party  is  engaged  in  mining  and  prospecting  about  a  quarter  of 
a  mile  east  of  the  preceding  diggings. 

Near  the  corner  of  towns  4  and  5,  ranges  2  and  3  east,  are  a  number  of  ranges  which 
have  been  worked  for  many  years.  Those  situated  on  section  one  are  the  property  of 
the  Mineral  Point  Mining  Company;  those  on  the  adjacent  sections  are  the  property  of 
Mr.  John  J.  Ross. 

There  are  six  principal  crevices,  running  nearly  parallel,  on  Sees.  36  and  1.  Their 
general  course  is  S.  70°  E.,  and  on  entering  Sec.  6,  they  run  nearly  east  and  west.  The 
crevices  lead  down  to  the  opening  between  the  Buff  and  Blue  limestones,  known  as  the 
glass-rock  opening.  The  ore  here  is  found  in  a  flat  sheet  about  a  foot  thick,  and  from 
70  to  140  feet  wide,  which  has  been  worked  for  a  distance  of  half  a  mile. 

The  ores  are  galenite  and  blende,  and  occur  associated  with  barite,  and  have  to  be 
separated  before  reduction. 

The  mode  of  drainage  in  Mr.  Ross'  mine  is  somewhat  peculiar.  Shafts  were  sunk  at 
intervals  to  a  depth  of  six  feet  below  the  opening,  into  the  Buff  limestone,  where  a  bei 
is  reached  through  which  the  water  readily  passes  away.  This  mode  of  drainage  was 
accidentally  discovered  in  prospecting  for  the  sheet.  No  ore  of  any  consequence  is  found 
in  the  upper  pipe-clay  opening;  occasional  bunches  have  been  found,  probably  not  over 
20,000  fcs.  in  all.  These  ranges  have  been  worked  at  intervals  for  the  last  forty  years 
by  various  parties.  Active  operations  were  commenced  by  Mr.  Ross  about  ten  years 
ago,  since  which  time  his  ground  has  produced  about  2,500,000  Ibs  of  lead  ore,  and 
about  3,500  tons  of  zinc  ores.  During  the  whole  time  in  which  these  mines  have  been 


736  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

worked,  it  is  safe  to  say  they  have  produced  not  less  than  eight  million  pounds  of  lead 
ore,  and  twice  as  much  zinc  ores.  During  the  winter  of  1874-5,  eight  men  were  em- 
ployed in  Mr.  Ross'  mines  and  produced  ore  to  the  value  of  $1,600.  During  the  winter 
of  1S75-6,  four  men  were  employed,  producing  ore  to  the  value  of  $1,000.  Work  will 
probably  be  resumed  this  winter. 

On  the  lands  of  the  Mineral  Point  Mining  Co.  several  parties  are  working  on  tribute. 
The  amount  this  ground  is  producing  could  not  be  ascertained. 

Goldsworthy  &  Bro.  These  diggings  are  situated  on  lots  279-280  of  Harrison's  sur- 
vey, about  a  quarter  of  a  mile  east  of  the  preceding  and  on  the  N.  W.  qr.  of  Sec.  6,  T. 
4,  R.  3  E.  This  is  known  as  the  Barber  range,  and  has  been  worked  in  the  winter 
season  during  the  last  six  years. 

The  ore  is  Sniithsonite,  much  mixed  with  pyrites;  it  is  found  in  the  upper  pipe-clay 
opening,  in  a  flat  sheet  from  8  to  30  feet  wide  and  from  18  to  24  inches  thick,  being 
most  productive  on  crossing  crevices. 

Four  men  are  employed  here  producing  about  20  tons  per  year. 

T.  Lutey  &  Co.  This  party  is  working  a  short  distance  east  of  the  preceding,  on 
land  owned  by  M.  M.  Cothren.  They  have  been  working  on  a  continuation  of  the  Bar- 
ber range  for  about  two  months  (October,  November,  1876)  and  have  now  a  very  good 
prospect. 

Most  of  the  lead  ore  from  the  Barber  range  is  obtained  from  the  glass-rock  opening, 
but  it  has  never  been  worked  for  zinc  ore.  ' 

Slithers  &  Co.  Situated  on  the  southeast  part  of  Harrison's  survey.  This  is  a  near- 
ly east  and  west  range,  known  as  the  "  Walla- walla,"  and  has  been  worked  by  the 
present  party  since  1865.  The  range  is  about  120  feet  wide  and  has  been  worked  in  the 
glass-rock  opening  to  a  length  of  about  1,000  feet,  and  at  a  depth  of  73  feet  below  the 
surface.  From  three  to  six  men  are  employed,  working  in  the  winter  season.  The 
mine  produces  lead  ore  and  both  kinds  of  zinc  ore.  The  average  annual  product  of 
lead  ore  is  about  44,000  pounds.  The  products  from  January  to  April,  1876,  of  all  kinds 
of  ore  were  valued  at  $900. 

J.  Arthur  &  Co.  Situated  on  the  S.  W.  qr.  Sec.  6,  T.  4,  R.  3  E.  This  is  an  east  and 
west  range,  discovered  about  two  years  since,  and  worked  continuously  to  the  present. 
The  ores  are  Sniithsonite  and  lead  ore,  found  in  a  flat  sheet,  from  six  inches  to  one  foot 
thick,  in  the  glass-rock  opening,  at  a  depth  of  60  feet  from  the  surface.  The  range  is 
about  100  feet  wide;  its  length  is  not  yet  known.  It  is  situated  on  land  owned  by  Mr. 
J.  J.  Ross.  The  ground  is  comparatively  dry. 

Hoare  Bros.  Situated  about  50  yards  east  of  the  preceding,  and  on  the  same  range, 
on  land  owned  by  Mr.  J.  Hoare.  This  party  has  been  working  here  about  two  years, 
producing  lead  ore  and  Sniithsonite  from  the  glass-rock  opening.  The  diggings  are  now 
very  good. 

Nichols  &  Holmes.  Situated  on  N.  E.  qr.  Sec.  7,  T.  4,  R.  3  E.,  a  short  distance 
east  of  the  old  zinc  works.  There  are  some  irregular  flat  sheets  of  zinc  ore  in  the  glass- 
rock  opening,  about  20  feet  deep.  They  have  been  worked  during  the  last  two  years 
and  have  produced  considerable  zinc  ore. 

Harris  &  Lang.  These  diggings  are  situated  about  half  a  mile  south  of  the  pre- 
ceding. This  is  an  east  and  west  range  situated  in  the  glass-rock  opening  about  25 
feet  deep.  It  has  been  worked  about  a  year,  producing  considerable  zinc  ore. 

In  the  vicinity  of  the  Mineral  Point  Town  Hall,  on  the  N.  W.  qr.  of  Sec.  5,  T.  4,  R.  3 
E.,  are  the  following  diggings: 

Prideaiix  &  Henry.  This  is  a  north  and  south  range,  about  200  yards  south  of  the 
Town  Hall,  which  has  been  worked  by  the  present  party  since  1866.  The  ores  are  lead 
und  zinc,  found  in  flat  and  pitching  sheets  from  8  to  10  inches  thick,  in  the  tipper  pipe- 


MINES  — MINERAL  POINT  DISTRICT.  737 

clay  opening,  at  a  depth  of  from  1  to  60  feet  below  the  surface.    The  range  is  from  60 
to  70  feet  wide,  and  has  been  worked  to  a  distance  of  350  feet. 

Jeffrey  &  Bro.  Situated  about  100  yards  south  of  the  preceding,  and  probably  on 
the  same  range.  The  range  is  here  100  feet  wide,  and  produces  lead  ore,  and  both  kinds 
of  zinc  ore,  in  about  equal  quantities,  and  considerable  iron  pyrites.  The  work  has  been 
chiefly  done  in  the  winter  season  during  the  last  two  years. 

Short  &  Foster.  Situated  about  200  yards  west  of  Jeffrey  &  Bro.,  on  an  old  north 
and  south  range,  sixty  feet  in  width.  They  have  been  working  during  the  last  two 
years  in  the  winter  season,  producing  lead  and  zinc  ores  from  the  pipe-clay  opening. 
The  diggings  are  about  40  feet  deep. 

Mankey  &  Son.  Situated  about  150  yards  S.  E.  of  Jeffrey  &  Bro.  They  have  been 
working  during  the  last  twelve  years  on  a  north  and  south  range.  The  product  is  lead 
ore  found  in  vertical  crevices,  and  in  flat  sheets  in  the  green-rock  opening  at  a  depth  of 
40  fdet  from  the  surface. 

All  the  diggings  on  this  hill  are  dry;  and  most  of  'them  are  remunerative,  but  the 
amounts  of  ore  produced  could  not  be  ascertained. 

The  mining  land  is  owned  by  Messrs.  Henry,  Goad,  Prideaux  and  Woodman. 

About  a  quarter  of  a  mile  north  of  this  ridge  is  the  Mineral  Point  Hill,  lying  di- 
rectly east  of  the  city.  The  following  parties  are  mining  there: 

Vivian  &  Sleep.  This  party  is  working  a  nearly  east  and  west  range,  the  most 
southeny  of  several  parallel  ranges  which  cross  the  hill.  The  range  is  about  50  feet 
wide,  and  produces  zinc  ores,  chiefly  Smithsonite,  from  the  upper  pipe-clay  opening, 
which  is  here  about  25  feet  below  the  surface.  They  have  been  working  here  during 
the  last  thirteen  years,  operating  during  the  entire  year. 

Brown  &  Glut  hers.  They  have  been  mining  about  a  year  on  a  parallel  range  150 
feet  north  of  the  one  last  mentioned.  The  range  is  about  50  feet  wide,  and  produces 
zinc  ores,  chiefly  blende.  The  ore  is  found  in  flat  and  pitching  sheets  in  the  pipe-clay 
opening. 

James  Dunn  &  Son.  This  party  has  been  working  about  three  years  on  a  range 
150  feet  north  of  the  preceding.  Both  kinds  of  zinc  ores  are  produced  from  the  upper 
pipe-clay  opening,  which  lies  here  about  40  feet  deep. 

Trewilla  &  Strong.  This  party  has  worked  about  eight  years  in  this  vicinity,  and 
one  and  a  half  years  on  their  present  range,  producing  zinc  ores. 

Goldsworthy  &  Hocks.  Situated  about  one-fourth  of  a  mile  east  of  Vivian  &  Sleep. 
They  have  been  mining  about  a  year,  producing  blende. 

The  mining  land  in  this  hill  is  owned  by  Messrs.  Hutchinson,  Henry,  Curry,  Gundry 
and  Washburn.  The  ranges  all  bear  a  little  north  of  west  and  south  of  east,  and  have 
never  been  worked  below  the  upper  pipe-clay  opening. 

The  earliest  mining  in  this  vicinity  was  done  on  the  Mineral  Point  Hill.  The  ranges 
were  formerly  very  productive,  and  have  been  worked  continuously  for  many  years  to 
the  present  time.  There  are  a  few  other  parties  mining  within  a  few  miles  of  Mineral 
Point.  They  are  as  follows: 

Rogers  &  3Iankey.  Situated  on  the  N.  E.  qr.  of  Sec.  8,  T.  4,  R.  3  E.,  on  land 
owned  by  Mr.  Suthers,  near  Rock  branch.  This  is  a  new  discovery  made  in  October, 
1876,  being  a  flat  sheet  of  Smithsonite  in  the  Brown-rock  opening. 

Jeffrey  &  May.  Situated  a  short  distance  north  of  the  preceding.  This  is  also  a 
new  discovery  made  about  the  same  time  as  the  preceding,  being  a  flat  sheet  of  zinc 
ores  in  the  glass-rock  opening.  The  prospect  is  very  good. 

Badcroft  Diggings.    Sec.  15,  T.  4,  R.  3  E.    Work  was  begun  here  in  1872,  and  has 
been  continued  at  intervals  since.    Three  men  have  been  employed,  chiefly  in  prospect- 
ing, and  a  small  amount  of  lead  ore  has  been  produced.    The  ore  is  found  in  flat  and 
pitching  sheets  in  the  pipe-clay  opening,  about  20  feet  below  the  surface. 
Wis.  SUK.— 47 


738  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

Shepard  &  Co.  Situated  on  the  N.  E.  qr.  of  the  N.  E.  qr.  of  Sec.  22,  T.  4,  R.  2  E. 
Work  was  commenced  here  in  August,  1876,  on  the  old  Maloney  range.  This  range 
has  a  general  east  and  west  course,  and  yields  lead  ore  and  blende  from  the  pipe-clay 
opening,  which  is  here  about  25  feet  deep.  The  ore  occurs  in  a  flat  sheet  from  4  to  5 
inches  thick,  the  blende  forming  the  top  and  bottom  of  the  sheet,  and  the  lead  ore  the 
central  part.  The  product  has  been,  to  December,  1876,  lead  ore,  1,500  pounds; 
blende,  3  tons.  The  ground  is  dry,  and  the  prospect  is  considered  good. 

Clebenstein  Diggings.  They  are  situated  on  the  same  ridge  and  a  short  distance 
east  of  the  preceding.  They  are  now  operated  by  August  Cain,  who  has  been  mining 
about  a  year.  They  were  operated  from  1865  to  1875,  by  Mr.  Clebenstein,  and  pro- 
duced large  amounts  of  lead  and  zinc  ores.  The  ore  was  found  in  flat  sheets,  in  the 
pip^-clay  and  glass-rock  openings. 

H.  Josephs  Diggings.  Situated  on  the  W.  hf .  of  the  S.  W.  qr.  of  Sec.  5,  T.  4,  R.  3 
E.  Mining  was  commenced  here  in  1871,  and  continued  until  the  fall  of  1874,  when  it 
was  discontinued  on  account  of  water.  The  ore  found  here  was  exclusively  blende, 
which  occurred  in  a  flat  sheet,  in  the  green-rock  opening.  The  width  of  the  sheet  was 
about-80  feet,  its  greatest  thickness  three  feet,  and  it  was  worked  for  a  distance  of  800 
feet.  The  greatest  depth  below  the  surface  is  70  feet.  During  the  years  187:3-4  this 
ground  produced  about  1,000  tons  of  blende. 

Diamond  Grove  Diggings. 

These  diggings  are  situated  on  Sees.  25  and  26,  T.  5,  R.  2  E.  They  produce  chiefly 
zinc  ores,  found  in  flat  sheets  in  the  pipe-clay  and  glass-rock  openings.  The  following 
parties  are  now  mining  here : 

Cain  &  Read.  Situated  on  the  N.  W.  qr.  of  Sec.  25.  This  party  has  been  working 
on  the  Rodersdorf  range  during  the  winters  of  1873-4  and  1874-5.  The  ore,  which  is 
Smithsonite,  is  found  in  the  glass-rock  opening,  in  a  range  from  16  to  20  feet  wide,  and 
200  feet  Jong.  The  production  during  the  first  season  was  17%  tons,  in  the  second  sea- 
son, 20  tons. 

Robert  Conley  &  Sons.  Situated  on  the  S.  W.  qr.  of  Sec.  25.  Mining  has  been 
carried  on  here  by  the  above  party  during  the  last  ten  years  on  an  east  and  west  range. 
Both  kinds  of  zinc  ore  and  lead  ore  are  found  here  in  the  pipe-clay  and  glass-rock  open- 
ings, but  chiefly  in  the  latter.  The  range  is  from  forty  to  sixty  feet  wide,  and  has  been 
worked  a  distance  of  150  yards.  During  the  last  year  and  a  half  the  product  of  lead 
ore  has  been  60/)00  pounds,  and  sixty  tons  of  zinc  ore  during  the  last  two  years. 

Biddick  Diggings.  A  valuable  deposit  of  lead  ore  has  lately  been  discovered  on 
the  S.  W.  qr.  of  Sec.  24,  T.  5,  R.  2  E.,  on  which  four  men  are  now  employed  running  a 
level.  Four  flat  sheets,  from  one  to  four  inches  thick,  are  found  here  situated  above 
one  another,  in  the  upper  pipe-clay  opening.  It  has  not  yet  been  sufficiently  worked  to 
determine  its  actual  extent. 

Martin  Bros.  &  Cramer.  Situated  on  the  S.  W.  qr.  of  Sec.  25.  This  and  the  pre- 
ceding are  on  land  owned  by  Mr.  James  Spensley.  They  have  been  mining  here  on  an 
east  and  west  range,  which  was  discovered  two  years  since.  The  ore  is  Smithsonite; 
and  is  found  in  the  glass-rock  opening,  which  is  here  from  ten  to  thirty  feet  deep. 

Spensley  &  Brown.  Situated  on  the  N.  E.  qr.  of  Sec.  26,  T.  5,  R.  2  E.  Six  men 
have  been  employed  here  since  July  1876  driving  an  adit  in  the  glass-rock  opening.  The 
adit  is  200  feet  long,  and  drains  an  east  and  west  range.  The  product  has  been,  lead 
ore,  36,000  pounds,  blende,  six  tons. 

Opir  &  Lancaster.  Situated  on  the  N.  W.  qr.  of  Sec.  26.  This  party  is  working 
the  same  range,  450  yards  west  of  the  preceding.  It  is  here  known  as  the  Lancaster 
range,  and  has  been  worked  by  the  present  party  about  a  year.  From  three  to  five  men 
are  employed,  and  the  product  has  been  150  tons  of  blende.  It  is  worked  by  an  adit. 


MINES  —  CALAMINE  DISTRICT.  739 

McDermott  &  Co.  Mining  has  been  carried  on  here  by  Mr.  McDennott  for  about 
26  years,  on  the  McShane  &  Gray  range.  The  ore  is  found  in  flat  and  pitching  sheet,  in 
crevices  and  crevice  openings  in  the  Galena  limestone  above  the  flat  openings.  The  dig- 
gings now  produce  lead  and  zinc  ore.  The  average  annual  product  is  about  30,000  Bos. 
Four  men  are  employed  here. 

Schlosser  &  Co.  This  party  has  been  working  four  or  five  years  on  the  east  end  of 
the  same  range  as  the  preceding.  The  ground  is  dry,  and  the  lead  ore  is  found  about 
40  feet  below  the  surface.  The  annual  product  is  about  10,000  S>s. 

Win.  and  Thos.  Thrasher.  This  party  has  worked  in  this  vicinity  about  fifteen  years, 
on  a  parallel  range  situated  about  a  quarter  of  a  mile  southeast  of  Schlosser  &  Co.  The 
product  is  chiefly  lead  ore. 

Lost  Grove  Diggings. 

These  diggings  are  situated  on  land  owned  by  Mr.  J.  J.  Ross,  on  Sec.  33,  T.  5, 
R.  2  E.  Mining  is  confined  here  to  the  winter  season.  The  ground  is  dry,  and  the  ore 
is  found  in  flat  sheet  in  the  glass-rock  opening.  The  following  parties  are  mining  here : 

Rigger  &  Arthur.  This  party  has  been  working  two  years  on  an  east  and  west 
range,  producing  lead  ore  and  Smithsonite.  The  range  varies  from  25  to  50  feet  in 
width,  and  lies  from  30  to  40  feet  below  the  surface.  The  product  is  valued  at  $1,200 
per  annum. 

Clayton  &  Co.  Situated  about  a  quarter  of  a  mile  northwest  of  the  preceding,  have 
been  working  during  the  last  twelve  years  on  the  Jim  Brown  range.  This  is  an  east 
and  west  range,  from  50  to  60  feet  wide,  and  lying  about  70  feet  below  the  surface,  pro- 
ducing exclusively  lead  ore.  The  product  has  been  about  20,000  pounds  per  annum. 

Garden  &  Son.  Situated  about  one-fourth  of  a  mile  south  of  the  preceding.  They 
have  been  working  about  two  years  and  have  produced  about  $400  worth  of  ore. 

Robert  Brown  &  Co.  Situated  about  half  a  mile  east  of  Clayton  &  Co.,  and  on 
the  same  range.  The  diggings  here  are  from  25  to  50  feet  deep.  They  have  been 
working  about  three  years  and  have  produced  about  30,000  pounds  per  annum. 

Furfer  &  Co.  They  have  been  working  on  a  range  near  Brown  &  Co.,  during  the 
last  eight  years,  producing  lead  and  zinc  ore. 

CALAMINE  DISTRICT. 

There  are  several  tracts  of  land  situated  fin  Sees.  18  and  19,  T.  3,  R.  3  E.,  which  were 
formerly  quite  productive;  but  little  work  is  now  done  on  them.  They  are  situated  on 
the  west  side  of  the  Pecatonica  river,  on  the  ridge  which  separates  the  Wood  and  Bon- 
ner  branches.  The  ridge  slopes  abruptly  on  all  sides  but  one  toward  the  various 
streams  which  nearly  inclose  it. 

On  the  summit  of  the  ridge  there  is  a  thickness  of  about  one  hundred  feet  of  Galena 
limestone,  underlaid  by  fifty  feet  of  the  Blue  and  Buff  limestones,  below  which  is  the 
sandstone.  All  these  formations  may  be  distinctly  seen  in  passing  from  the  summit  of 
the  ridge  to  the  valley  of  the  Pecatonica. 

During  the  winter  of  1876-7  some  mining  was  done  here  by  Mr.  Charles  Mappes,  of 
Belmont,  on  an  east  and  west  range  lying  from  30  to  40  feet  below  the  surface.  Four 
men  were  employed,  working  on  a  flat  sheet  of  blende  and  galenite.  The  amount  pro- 
duced could  not  be  ascertained.  Some  Smithsonite  is  also  produced  in  this  vicinity. 

Yellowstone  Diggings. 

Pierce  &  Son.  Some  work  has  been  done  here  during  the  winter  seasons  of  the  last 
three  years,  in  a  range  a  quarter  of  a  mile  north  of  the  Newkirk  range,  situated  on  the 
S.  W.  qr.  of  Sec.  14,  T.  4,  R.  4  E.  The  lead  ore  is  found  in  a  vertical  sheet  in  a  crevice 
opening  about  fourteen  feet  below  the  surface.  In  the  winter  of  1874-5  the  product 


740     GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

was  18,000  pounds,  and  in  the  following  winter  about  1,800  pounds.    No  mining  is 
done  here  in  the  summer. 

WIOTA  DISTRICT. 

This  is  a  small  group  of  east  and  west  ranges,  crossed  by  north  and  south  crevices, 
situated  in  the  N.  W.  qr.  of  Sec.  19,  T.  2,  R.  5  E.  But  very  little  mining  is  done  here; 
the  annual  production  of  the  whole  district  does  not  exceed  40,000  pounds.  The  ore  is 
lead,  occurring  in  the  middle  portion  of  the  Galena  limestone,  and  there  does  not  seem 
to  be  any  regular  opening.  There  are  several  parties  here,  among  whom  the  principal 
ones  are  as  follows : 

Piircell  &  Harden.  They  are  at  work  in  the  old  Hamilton  diggings,  removing  the 
pillars  from  the  old  workings  which  were  abandoned  many  years  since.  They  are  un- 
able to  go  any  deeper,  or  make  any  new  discoveries,  on  account  of  water,  which  is  here 
quite  plentiful.  The  ground  is  owned  by  the  Ridgeway  Mining  Co.,  of  Madison. 
Messrs.  Purcell  &  Harden  have  worked  here  two  years,  and  during  that  time  have  pro- 
duced 20,000  pounds  of  lead  ore. 

Smith  &  Anderson.  Situated  a  short  distance  north  of  the  preceding,  and  form  the 
northern  part  of  the  Hamilton  diggings.  This  does  not  appear  to  form  any  regular 
range.  The  ore  occurs  in  east  and  west  sheets,  in  very  hard  rock,  and  seldom  in  open- 
ings, the  diggings  have  now  been  worked  since  January,  1873,  and  have  produced 
80,000  pounds. 

MONROE  DISTRICT. 

These  are  the  most  easterly  diggings  in  the  lead  region,  and  are  chiefly  interesting  for 
that  reason.  They  are  situated  about  three  miles  and  a  half  north  of  the  city  of  Mon- 
roe. At  present  only  two  parties  are  at  work. 

T.  H.  White  &  White.  Situated  on  the  N.  E.  qr.  of  Sec.  14,  T.  2,  R.  7  E. 
The  ore  is  found  here  in  a  flat  sheet,  accompanied  by  pipe  clay,  about  twenty- three 
feet  below  the  surface.  The  general  course  of  the  sheet  is  northwest  and  southeast 
and  produces  only  lead  ore.  The  ground  is  quite  free  from  water.  The  present  parties 
have  been  working  here  six  years,  during  which  period  they  have  produced  90,000 
pounds  of  lead  ore. 

Frame  &  Co.  Situated  on  the  S.  E.  qr.  of  Sec.  10,  T.  2,  R.  7  E.,  on  the  land  of 
Mr.  Henry  Wilber.  This  is  an  east  and  west  range,  about  half  a  mile  northeast  of  the 
preceding.  It  was  discovered  in  1844,  and  has  been  proved  for  a  distance  of  700  feet. 
The  lead  ore  is  found  in  both  vertical  crevices  and  flat  openings.  There  appear  to  be 
three  principal  vertical  crevices,  connected  in  places  by  horizontal  sheets. 

They  were  worked  by  Mr.  John  Monahan,  from  1870,  to  February,  1872,  chiefly  in 
the  winter  season,  during  which  time  he  produced  50,000  pounds.  Mr.  Frame  took  the 
ground  in  1874,  and  produced  4,000  pounds  in  the  first  six  months.  The  production 
since  then  could  not  be  ascertained.  The  ground  is  quite  dry,  and  the  workings  are 
about  fifty  feet  below  the  surface. 

It  is  not  probable  that  any  extensive  deposits  exist  in  this  vicinity.  The  ground  ap- 
pears rather  to  be  such  as,  by  careful  working,  will  afford  moderate  wages  to  a  few 
persons. 


COPPER  IN  THE  LEAD  REGION. 


COPPER  IN  THE  LEAD  REGION". 

At  present  no  mining  for  copper  is  done  in  the  lead  region,  nor  has  there  been  for 
several  years,  except  at  Mineral  Point  in  the  years  1873  to  1876.  Indications  of  its  pres- 
encs  are  found  in  many  places  through  the  mines,  as  an  associate  mineral  in  the  lead 
*rtns.  The  most  systematic  attempt  at  copper  mining  was  made  at  Mineral  Point. 

Mr.  James  Toay,  who  is  well  acquainted  with  the  past  history  of  the  enterprise  has 
kindly  furnished  the  following  statement: 

"  Sometime  in  the  year  1837  or  1838,  copper  was  first  discovered  on  the  S.  E.  qr.  of 
Sec.  32,  T.  5,  R.  3  E.,  one  mile  northeast  of  the  Mineral  Point  court  house.  The  crev- 
ice had  a  course  S.  85°  E.,  and  had  been  traced  for  over  one-third  of  a  mile.  This  lo- 
cality has  not  been  worked  since  1842.  A  great  amount  of  copper  was  obtained. 

"  It  is  reported  that  over  one  and  a  half  million  pounds  of  copper  were  taken  out, 
which  would  include  all  kinds  of  ore:  '  Smalls,'  which  would  not  yield  more  than  ten 
to  fifteen  per  cent  of  copper;  and  the  stone  or  '  Prill'  ore,  yielding  twenty-five  to  thirty 
per  cent. 

"  Some  of  the  ore  was  smelted  at  the  old  furnace  owned  by  William  Kendall  &  Co., 
and  some  fit  the  new  Baltimore  furnace,  owned  by  Ansley  &  Co.  About  50,090  pounds 
was  sent  to  England  or  Wales  for  reduction,  which  indicates  that  parties  here  did  not 
at  that  time  understand  the  proper  method  of  smelting  copper.1 

"  Sometime  in  1844,  S.  P.  Preston  came  here,  and  went  into  partnership  with  Kendall 
&  Co.,  and  after  that  they  had  no  trouble  in  smelting  copper  successfully. 

"The  amount  of  copper  sold  from  Kendall  &  Co.'s  furnace  from  1841  to  1846  was 
217,702  ft>s.  This  was  about  ninety-five  per  cent,  pure  copper,  and  sold  for  fourteen 
cents  per  pound. 

"Two  other  furnaces  have  been  worked;  one  by  Charles  Bracken,  to  what  extent  I 
have  no  knowledge,  but  know  he  smelted  considerable  copper  ore  from  his  own  land. 
The  other  was  owned  by  Curtiss  Beach.  Here  a  great  amount  of  copper  ore  was  smelt- 
ed, taken  from  the  Beach  diggings.  The  greatest  amount  of  ore  that  Kendall  &  Co. 
smelted  was  taken  from  the  Kendall  diggings. 

"  It  is  probable  that  with  the  increased  advantages  in  the  present  price  of  copper;  in 
obtaining  coke  instead  of  charcoal  for  smelting,  and  in  shipping  facilities,  that  copper 
mining  may  now  be  made  a  profitable  business  at  this  place  if  properly  managed. ' ' 

During  the  years  1873,  1874  and  1875,  about  200  tons  of  copper  ore  were  produced  by 
Mr.  Toay  from  the  mines  near  Mineral  Point.  An  attempt  was  also  made  to  smelt  it 
in  1874.  No  very  large  amount  was  smsltsd,  as  the  common  blast  furnace  was  not  ex- 
actly adapted  to  its  reduction.  The  ore  is  a  sulphuret  of  copper.  The  exact  amount 
produced  could  not  be  learned. 

The  ranges  referred  to  in  the  foregoing  statement  of  Mr.  Toay  are  situated  as  follows : 

Ansley  Range.  Course  S.  85°  E.,  running  from  the  center  of  Sec.  32,  T.  5,  R.  3  E., 
one-third  of  a  mile  long. 

Keiidal  Range.  N.  E.  qr.  of  Sec.  5,  and  N.  W.  qr.  of  Sec.  4,  T.  4,  R.  3  E.,  run- 
ning from  near  the  quarter  post  of  Sees.  5  and  32,  nearly  to  the  center  of  Sec.  4.;  length, 
about  two  thousand  feet. 

Beach  Range.  E.  hf .  of  Sec.  4,  T.  4,  R.  3  E.  Crossing  the  center  line  of  Sec.  4  one- 
quarter  of  a  mile  east  of  the  center  of  the  section,  and  running  600  feet  from  that  point 
on  a  course  N.  85°  W.,  and  600  feet  on  a  course  S.  85°  E. 

i  Two  specimens  of  copper  ore  from  the  Mineral  Point  district,  S.  E.  qr.  of  Sec.  33,  T.  5,  R.  3  E., 
were  analyzed  with  these  results:  No.  1  gave  metallic  copper,  38.78  per  cent.  No.  2  gave  copper, 
4.48  per  cent. 


742  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

Wasley  Range.  S.  W.  qr.  of  the  S.  E.  qr.  of  Sec.  32,  T.  5,  R.  3  E.  Course  S.  85° 
E.;  length,  about  1,000  feet. 

Ballard  Range.  S.  E.  qr  of  the  S.  E.  qr.  of  Sec.  32,  T.  5,  R.  3  E,  Course  N.  30° 
E.;  length,  about  800 feet. 

Besides  these  there  are  several  small  north  and  south  ranges  on  the  N.  E.  qr.  of  the 
N.  W.  qr.  of  Sec.  5,  T.  4,  R.  3  E. 

Traces  of  copper  ore  are  also  found  at  many  points  north  of  Mineral  Point,  in  the 
diggings  between  that  city  and  Dodgeville. 

A  specimen  of  ore  containing  a  considerable  carbonate  of  copper  was  presented  by 
Hon.  H.  H.  Gray,  of  Dodgeville.  It  was  found  about  fifteen  feet  from  the  surface,  on 
the  S.  W.  qr.  of  Sec.  22,  T.  2,  R.  3  E. 

Specimens  of  sulphuret  of  copper  were  obtained  from  some  old  diggings  on  the  S. 
W.  qr.  of  Sec.  8,  T.  1,  R.  5  E.  The  course  of  this  range  is  about  S.  20°  E.  Copper 
was  mined  here  as  early  as  1838,  and  two  or  three  loads  of  ore  were  brought  to  Mine- 
ral Point  for  reduction.  A  specimen  from  this  locality  afforded  10.86  per  cent,  of  metal- 
lic copper. 

STATISTICS  OF  ZINC  OKE. 

The  statistics  of  the  production  of  zinc  ores  are  believed  to  be  complete,  and  to  em- 
brace the  annual  production  from  the  year  1860  (at  which  time  the  zinc  ores  began  to 
be  utilized)  to  October,  1876.  The  ore  is  all  consumed  at  La  Salle,  111.,  by  four  com- 
panies. By  far  the  greatest  quantity  of  the  ore  is  shipped  from  Mineral  Point;  the  other 
points  are  Platteville,  Council  Hill,  and  Galena. 

The  blende  is  shipped  in  its  crude  state,  as  it  comes  from  the  mines;  but  the  carbo- 
nate of  zinc  (drybone)  is  previously  roasted  or  calcined,  by  which  process  it  loses  its 
carbonic  acid,  which  constitutes  about  one-third  of  its  weight,  and  is  decreased  in  bulk 
in  the  same  ratio.  The  small  amount  of  water,  which  is  usually  present  as  a  mechani- 
cal mixture  with  the  ore,  is  also  driven  off. 

The  ore  is  calcined  in  a  small  and  inexpensive  furnace,  resembling  a  lime-kiln  in  its 
structure  and  object,  capable  of  containing  about  sixty  tons  of  raw  ore.  Such  a  furnace 
will  roast  about  twenty-five  tons  of  ore  in  twenty-four  hours,  and  requires  the  labor  of 
six  men  at  eight  hours  apiece  (three  shifts).  From  eighty  to  one  hundred  pounds  of 
bituminous  coal  are  required  for  each  ton  of  ore. 

The  cost  of  carrying  the  ore  through  this  operation  is  from  fifty  to  sixty  cents  per  ton. 
The  coet  of  a  furnace  and  requisite  tools  is  about  $300. 

The  following  are  the  amounts  of  zinc  ores  produced  in  the  lead  region  from  1860  to 
October  1,  1876.  The  table  has  been  prepared  from  the  books  of  the  four  manufacturing 
companies,  to  whom  I  am  greatly  indebted  for  their  ready  cooperation  and  assistance: 

Smithtonite,  Blende, 

Year.                                                                                       Ibs.  Ibs. 

1860 320,000  

1861 266>000      

1862 

1863 1,120,000      

1884 3,173,333      

1865 4,198,200      

1866 7,373,333      

1867 5,181,445  841,310 

1868 4,302.383  3,078-,4.T5 

1869 4,547,971  6,252,420 


PLATE,XXXII 


O  UTLI  N  E   M  A  P 

«/'////» 

IYE  AD     R  E  CV  1  O  X 

jig  t/ir  several  J/r'n  i  riff  Districts 


STATISTICS  OF  THE  PRODUCTION  OF  LEAD  ORE. 


743 


Smithsonite, 

Tear.  Ms. 

1870 4,429,585 

1871 16,618,160 

1872, 27,694,574 

1873 20,538,946 

1874 15,123,050 

1875 11,878,210 

1876,  to  October  1st 12,168,540 

Total 138,933,730 


Blende, 

Ibs. 

7,414,022 
9,303,625 
16,256,970 
15,089,514 
19,500,465 
20,538,190 
17,181,490 

115,456,441 


The  following  statistics  of  the  shipment  of  ores  and  metals  over  the  Mineral  Point 
railroad  were  furnished  through  the  kindness  of  Mr.  C.  Spensley,  of  Mineral  Point: 


Year. 

1857 

1858 

1859 

1860 

1861..., 

1862 

1863 

1864 

1865 

1866 

1867 

1868 

1869 

1870 

1871 

1872 

1873 

1874 

1875 

1876,  to  October  1, 


Lead,  Ibs. 
1,780,490 
3,451,539 
2,991,925 
3,548,335 
2,360,663 
2,511,161 
2,180,570 
1,763,769 
2,708,478 
1,837,720 
2,854,000 
2,854,397 
1,948,000 
4,352,400 
3,027,520 
3,577,777 
1,972,230 
3,077,020 
2,632,940 
2,402,000 


Zinc  Ores,  Ibs. 


240,000 
200,000 

840,000 

2,380,000 

3,148,650 

5,380,000 

2,660,000 

4,484,000 

8,780,000 

12,740,000 

21,140,000 

30,900,000 

27,414,000 

28,022,000 

31,538,000 

23,538,000 


Spelter,  Ibs.    Lead,  White,  Ibs. 


103,400 
701,210 
630,580 


67,510 

983,010 

1,317,370 

1,360,000 


These  estimates  will  include  the  greater  part  of  the  pig  lead,  and  the  zinc  ores  pro- 
duced in  the  northern,  central,  and  eastern  parts  of  the  Lead  region;  and  all  the  spelter 
and  zinc  white  produced  at  the  old  Mineral  Point  Zinc  Works,  which  have  lately  been 
torn  down  and  sold. 

The  statement  of  zinc  ores  shipped  by  the  railroad  is  much  too  small  to  represent  tho 
true  production  of  this  part  of  the  Lead  region,  as  no  allowance  is  made  for  overloading 
the  cars,  and  for  calcination,  which  would  make  the  amount  fully  one-fourth  greater. 


STATISTICS  OF  THE  PKODUCTION  OF  LEAD  OEE 

in  tlie  Lead  Beg  ion,  from  January  1,  1862,  to  October  1,  1876. 

During  the  progress  of  this  survey,  much  time  and  care  have  been  devoted  to  this 
portion  of  the  work,  in  writing  to  and  personally  soliciting  information  from  all  persons 
possessed  of  it,  and  especially  from  the  smelters.  We  have  sought  to  prepare  a  state- 
ment of  the  amount  of  lead  ore  produced  annually  in  each  district,  and  a  conbimed  esti- 
mate of  the  total  amount  for  the  Lead  region. 


744  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

Had  it  been  possible,  it  would  have  been  preferable  to  prepare  the  statement  of  each 
district  from  the  mines  therein  contained;  but  it  is  seldom  that  a  written  account  has 
been  kept  by  the  owners,  of  the  lead  ore  produced  from  any  range,  mine,  or  diggings, 
extending  back  a  sufficient  number  of  years  to  furnish  the  information  required. 

Statements  of  the  production  of  individual  mines  and  ranges  have  been  frequently 
furnished,  and  when  they  were  believed  to  be  reliable,  they  have  been  incorporated  in 
the  preceding  part  of  the  report.  Such  statements,  however,  are  usually  based  on  the 
memory  of  the  persons  who  give  them,  and  are  therefore  somewhat  liable  to  error. 

The  lead  ore  produced  in  each  district  is  seldom  exported  from  it  as  such,  but  is 
usually  reduced  by  the  furnaces  of  that  district,  and  then  exported  as  pig  lead.  There- 
fore it  was  believed  that  the  most  accurate  statistics  could  be  obtained  from  the  books 
of  the  smelters;  accordingly  circular  letters  have  been  sent  to  each  of  them,  to  which 
in  most  instances  they  immediately  responded,  giving  a  full  and  complete  statement 
taken  directly  from  their  books,  and  leaving  nothing  further  to  be  desired.  Some  were 
unable  to  do  so,  as  their  old  accounts  were  lost  or  mislaid,  and  some,  perhaps,  were  un- 
willing to  have  a  detailed  statement  of  their  business  published.  All  who  did  not 
respond  to  -the  circular  were  personally  visited,  and  a  statement  giving  the  general 
average  obtained.  Although  some  of  the  individual  statements  herewith  submitted 
may  be  liable  to  slight  error,  yet  it  is  confidently  believed  that  the  estimates  are,  as  a 
whole,  rather  too  small  than  too  large;  and  that  they  are  as  reliable  as  it  is  now  possible 
to  make  them.  We  are  thus  enabled  to  give  the  products  of  the  separate  parts  of  the 
district,  and  a  total  of  the  whole. 

In  presenting  these  statistics,  besides  the  product  of  the  furnace,  some  remarks  will 
be  added  as  to  the  localities  of  the  mines  which  form  its  supply,  and  the  number  and 
kind  of  furnaces. 

BEETOWN  DISTRICT. 

Commencing  in  the  western  portion  of  the  Lead  region  and  proceeding  eastward,  the 
first  is  the  Beetown  furnace,  in  which  is  smelted  all  the  ore  of  the  Beetown  diggings, 
together  with  that  of  Muscalonge,  Nip  and  Tuck  and  Hackett's  diggings. 

The  furnace  is  owned  and  operated  by  Hon.  Christopher  Hutchinson,  by  whom  it  was 
built  in  1868.  Previous  to  that  time,  all  of  the  ore  of  the  above  mentioned  district  was 
smelted  at  Potosi.  It  is  a  reverberatory  furnace,  known  as  a  Drummond,  with  a  capa- 
city of  9,000  pounds  of  ore  in  twenty-four  hours. 

It  consumes  one  and  three-fourths  cords  of  oak  wood,  and  is  operated  by  two  men. 
The  number  of  pounds  of  lead  ore  smelted,  from  June  19,  1868,  to  October  1,  1876,  is 
as  follows: 

Yecr.                                  Pounds  of  Ore.  Tear.                               Pounds  of  Ore. 

1868 800,000           1873 850,000 

1869 1,100,000           1874 1,000,000 

1870 1,700,000           1875 800,000 

1871 1,300,000           1876 700,000 

1872 900,000 

Total 9,150,000 


PLATTEVILLE  DISTRICT. 

Proceeding  eastward,  the  next  is  the  Platteville  district,  which  has  two  furnaces,  both 
near  the  village.  Here  is  smelted  all  the  ore  raised  in  the  Platteville  and  Whig  dig- 
gings; and  also  that  from  Big  Patch  in  the  town  of  Smelser: 


STATISTICS  OF  THE  PRODUCTION  OF  LEAD  OHE. 


Tear.  Furnace  No.  1. 

1862 800,000 

1863 600,000 

1864 600,000 

1865 500,000 

1866 500,000 

1867 500,000 

1868 450,000 

1869 450,000 

1870 450,000 

1871 600,000 

1872 600,000 

1873 400,000 

1874 500,000 

1875 504,000 

1876 1,044,000 


Furnace  No.  2. 
350,000 
350,000 
350,000 
350,000 
350,000 
350,000 
350,000 
350,000 
350,000 
3-50,000 
350,000 
200,000 


Total. 

1,150,000 
950,000 
950,000 
850,000 
850,000 
850,000 
800,000 
800,000 
800,000 
950,000 
950,000 
600,000 
500,000 
504,000 

1,044,000 


Total 8,498,000 


4,050,000 


12,548,000 


The  above  table  gives  in  round  numbers  the  product  of  the  Platteville  district  since 
1861;  it  is,  however,  only  an  approximation  made  by  the  smelters  themselves,  and  be- 
lieved to  be  tolerably  correct.  Furnace  No.  1,  owned  by  Messrs.  Straw  &  Spensley,  is  a 
blast  furnace  having  two  hearths,  and  is  situated  about  half  a  mile  south  of  the  village. 

Furnace  No.  2,  owned  by  Mr.  Coates,  is  situated  near  the  railroad  depot.  It  is  a  blast 
furnace  of  two  hearths,  and  has  not  been  worked  since  some  time  in  1873.  Nothing 
more  than  a  verbal  statement  of  its  annual  average  could  be  obtained. 

POTOSI  DISTRICT. 

There  have  been,  at  various  times  since  1861,  four  furnaces  operating  in  the  vicinity, 
of  which  only  two  are  now  worked.    They  are  as  follows,  in  kind  and  condition: 
Vance's  Furnace  ceased  work  in  1868 

Gibson  &  Co.  ceased  work  in  -      1871 

A.  W.  Emery's  furnace,  situated  near  Rockville,  is  a  reverbatory,  with  a  capacity  of 
6,000  pounds  to  every  24  hours.  Thomas  Hymer  &  Co.'s  furnace,  situated  near  British 
Hollow,  is  a  blast  furnace  of  one  hearth. 

Previous  to  1868,  all  the  ore  from  the  Beetown  district  was  smelted  at  these  furnaces, 
in  addition  to  that  which  they  now  smelt,  which  comprises  the  mines  of  Potosi,  British 
and  Dutch  Hollows,  and  Rockville. 

A  detailed  statement  of  the  ore  smelted  at  the  several  furnaces  could  not  be  obtained, 
but  from  the  verbal  statements  of  the  several  smelters,  the  following  estimate  has  been 
prepared  which  is  believed  to  be  nearly  correct: 


Povnds  oj  Lead 
Year.  Ore  Smelted. 

1862 6,050,000 

1863 5,120,000 

1864 4,500,000 

1865 5,200,000 

1866 4,400,000 

1867 3,500,000 

1868 2,600,000 

1869 2,200,000 


Pounds  of  Lead 
Tear.  Ore  Smelted. 

1870 1,900,000 

1871  2,230,000 

1872 1,400,000 

1873 1,500,000 

1874 750,000 

1875...., 700,000 

1876  to  Oct.  1st 650,000 


Total  from  January  1,  1862  to  October  1,  1876 42,700,000 


746  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

HAZEL  GREEX  DISTRICT. 

This  district  embraces  all  of  the  mines  in  the  vicinity  of  the  village  of  Hazen  Green, 
and,  indeed,  all  the  ore  produced  between  the  Sinsinawa  river  and  the  Coon  branch  of 
the  Galena  river. 

The  furnace  is  a  new  blast-furnace  of  one  hearth,  and  a  capacity  of  100  pigs  (of  70 
pounds  each),  in  twenty-four  hours.  It  is  owned  and  operated  by  Messrs.  Crawford, 
Mills  &  Co.,  who  furnished  the  following  statement  from  their  books.  It  is  situated  on 
the  Hard  Scrabble  branch,  about  a  mile  southeast  of  the  village  of  Hazel  Green. 

Pounds  of  Lead  Pounds  of  Lead 

Year.                                    Ore  smelted.  Year.                                          Ore  smelted. 

1862 2,027,047  1870 1,223,250 

1863 1,262,640  1871.... 1,230,917 

1864 837,597  1872 1,278,524 

1865 753,821  1873 1,046,626 

1866 797,421  1874     830,174 

1867 1,334,640  1875   735,395 

1868 1,541,670  1876,  to  October  1st 723,193 

1869  1,315,970 

Total  from  January  1,1862  to  October  1,  1876   16,938,885 


NEW  DIGGINGS  DISTRICT. 

This  district  embraces  the  diggings  in  the  vicinity  of  the  village;  all  east  of  the  Coon 
branch  of  Galena  river  as  far  as  T.  1,  R.  2  E.,  and  the  mines  in  the  vicinity  of  Benton. 

The  furnace  is  a  blast  of  two  hearths,  and  is  known  as  the  Democrat  furnace.  It  is 
situated  about  two  miles  north  of  New  Diggings.  It  was  worked  from  1864  to  1869  by 
Mr.  Geo.  Wilde,  of  Dubuque,  and  since  then  has  been  worked  by  T.  G.  Stevens  &  Co. 

Pounds  of  Lead  Pounds  of  Lead 

Year.  Ore  smelted.  Year.  Ore  smelted. 

1862 1,050,000  1870 2,200,000 

1863 1,200,000  1871 1,700,000 

1864 1,125,000  1872 1,650,000 

1865 1,200,000  1873 1,128,000 

1866 1,100,000  1874 1,200,000 

1867 1,150,000  1875 1,200,000 

1868 1,200,000  1876,  to  October  1st....     1,300,000 

1869 1,100,000 

Total  from  January  1,  1862,  to  October  1,  1876 19,503,00) 


In  addition  to  this,  there  was  smelted  at  the  Jefferson  furnace,  by  T.  G.  Stephens  & 
Co.,  as  follows: 

Pounds  of  Ore  Pounds  of  Ore 

Year.  smelted.  Year.  smelted. 

1862 1,098,938  1866 1,073,415 

1863 1,326,193  1867 1,050,597 

1864 1,112.095  1868 1,429,158 

1865 1,078,609  1869 1,515,323 

Total 9,684,333 


The  furnace  used  was  a  Drummond,  with  a  capacity  of  7,000  Ibs.  per  twenty-four  hours. 


STATISTICS  OF  THE  PRODUCTION  OF  LEAD  ORE. 


747 


SHULLSBURG  DISTRICT. 

The  mines  embraced  in  this  district  are  situated  in  T.  1,  R.  2  E.,  and  some  in  the 
eouth  part  of  T.  2,  R.  2  E.,  being  not  a  very  large  but  quite  productive  district. 

There  are  two  furnaces  in  operation  in  the  district.  No.  1  is  now  operated  by  Mr.  B. 
Spensley,  of  Shullsburg,  and  was  formerly  owned  and  operated  by  Messrs.  Quinch  & 
Estey,  of  that  place.  It  is  a  blast  furnace  of  two  hearths,  situated  a  short  distance 
west  of  the  village,  on  the  Shullsburg  branch.  No.  2  is  also  a  blast  furnace  of  two 
hearths,  capable  of  smelting  12,000  pounds  of  ore  in  twenty-four  hours,  with  six  men. 
It  is  also  situated  near  the  Shullsburg  branch,  about  four  miles  below  Shullsburg.  Prior 
to  June  1st,  1873,  it  was  operated  by  Messrs.  Joseph  Hutchinson  &  Sons.  At  that  time 
it  was  leased  to  Mr.  Wesley  Spensley,  for  a  term  of  three  years,  and  is  now  operated  by 
Messrs.  Spensley  &  Hutchinson.  A  full  account  has  been  furnished  of  their  production. 


Year. 


Pounds  of  Lead 
Ore  smelted  at 
furnace  N~o,  1. 

1862 1,000,000 

1863 1,000,000 

1864 1,000,000 

1865 1,000,000 

1866 1,000,000 

1867 1,000,000 

1868 1,000,000 

1869 1,000,000 

1870 1,463,986 

1871 1,250,362 

1872 1,146,448 

1873 1,084,221 

1874 1,000,000 

1875 • 900,000 

1876,  to  Oct.  1st 625,000 


Total 15.470,017 


Pounds  of  Lead 

Ore  smelted  at 

Furnace  No.  2. 

800,000 

700,000 

400,000 

1,000,000 

1,000,000 

1,200,000 

700,000 

200,000 

400,000 

400,000 

300,000 

250,000 

700,000 

900,000 

1,000,000 

9,950,000 


Total. 

1,800,000 
1,700,000 
1,400,000 
2,000,000 
2,000.000 
2,200,000 
1,700,000 
1,200,000 
1,863,986 
1,650,362 
1,446,448 
1,334,221 
1,700,000 
1,800,000 
1,625,000 

25,420,017 


MINERAL  POINT  DISTRICT. 

The  ore  smelted  at  the  Mineral  Point  furnaces  is  derived  from  all  the  mines  and  dig- 
gings in  the  vicinity  of  the  city.  Ore  is  also  brought  here  in  many  cases  from  long  dis- 
tances. The  ore  of  the  following  districts  is  also  smelted  here,  viz:  Mifflin,  Linden,  Lost 
Grove,  Diamond  Grove,  Duke's  Prairie,  and  Wiota. 

There  are  two  furnaces  now  in  operation.  No.  1  owned  by  Mr.  James  Spensley  is 
situated  one  mile  west  of  the  city,  on  the  Spensley  branch  of  the  Pecatonica.  It  is  a 
reverberatory,  with  a  capacity  of  6,500  Ibs.  per  day.  There  is  also  a  blast  furnace  here 
of  two  hearths,  but  it  is  seldom  used,  except  for  smelting  slag  and  large  ore. 

Furnace  No.  2,  is  situated  about  a  mile  above  No.  1,  on  the  same  stream,  and  is  ope- 
Tated  by  Mr.  John  Spensley.  There  is  here  a  blast  furnace  of  three  hearths,  and  a  re- 
verberatory. The  latter  is  the  only  one  now  used. 

A  full  statement  has  been  given  by  Mr.  James  Spensley  of  furnace  No.  1,  and  is  in- 
serted below,  with  the  exception  of  the  years  1862  and  1863,  which  have  been  estimated 
irom  an  average  of  the  others.  The  amount  of  ore  smelted  at  furnace  No.  2,  from  1863 
to  1872  inclusive,  is  estimated  by  Mr.  John  Spensley  at  7,273,764  Ibs.  As  the  annual 


748 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


product  in  this  district  has  been  comparatively  uniform,  the  average  annual  product 
may  be  estimated  at  one-tenth  of  it. 
The  production  of  the  Mineral  Point  District  will  then  stand  as  follows : 

Total. 
1,991,938 
1,991,938 
1,683,998 
1,889,058 
2,154,058 
2,043,608 
2,252,710 
2,532,710 
2,192,306 
1,990,672 
1,661,376 
1,518,888 
1,850,000 
2,000,000 
1,455,350 


Year. 

furnace  No.  1. 

Furnace  No.  2. 

1862  

1,264,562 

727,376 

1863  

1,264,562 

727,376 

1864  

956,622 

727,376 

1865  

1,161,682 

727,376 

1866  

1,426,682 

727,376 

1867  

....   1,316,232 

727,376 

1868  

1,525,3:34 

727,376 

1869  

1,805,334 

727,376 

1870  

1,464,930 

727,376 

1871  

1,263,296 

727,376 

1872  

934,000 

727,376 

1873  

791,512 

727,376 

1874  .. 

900,000  ' 

950,000 

1875  

900,000 

1,100,000 

1876,  to  Oct.  1st  

755,350 

700,000 

Total  

17,730,098 

11,478,512 

29,208,610 


DODGEVILLE  DISTRICT. 

This  district  comprises  all  the  mines  in  the  vicinity  of  the  village  of  Dodgeville,  Van 
Meter's  survey,  and  all  ore  raised  north  and  east  of  Dodgeville. 

There  are  two  reverberatory  furnaces  here.  No.  1  is  owned  and  operated  by  Messrs. 
Hendy  &  Mundy,  and  has  a  capacity  of  6,000  pounds  per  day.  This  furnace  com- 
menced work  in  1869.  No.  2  is  owned  by  Messrs.  Bennett  &  Georges,  and  has  a  capac- 
ity of  7,500  pounds  per  day.  Both  are  situated  a  short  distance  north  of  the  village. 
Full  statements  have  been  received  from  furnace  No.  1,  and  from  furnace  No.  2,  \vith 
the  exception  of  the  last  three  years,  which  have  been  estimated. 

Total. 
1,369,989 
1,055,441 
905,511 
866,407 
1,154,298 
1,191,939 
1,046,081 
1,162,718 
1,374.617 
1,932,259 
1,836,320 
1,441,999 
1,595,000 
1,240,000 
1,100,000 


Year. 

Furnace  No.  1. 

Furnace  No.  2. 

1862  

1,369,989 

1863  

1,055,441 

1864  

905,511 

1865  

866,407 

1866  

1,154,298 

1867  

,  1,191,939 

1868  

1,046,081 

1869  

184,000 

978,718 

1870  

435,000 

939,617 

1871  

737,000 

1,195,259 

1872  

934,000 

902,320 

1873  

626,000 

815,999 

1874  

695,000 

900,000 

1875  

340,000 

900,000 

1876,  to  October  1st  

400,000 

700,000 

Total 4,351,000 


14,921,579 


19,272,579 


STATISTICS  OF  THE  PRODUCTION  OF  LEAD  ORE. 

HIGHLAND  DISTRICT. 

This  district  comprises  the  mines  in  the  vicinity  of  Highland,  Centerville,  and  the 
Crow  Branch  diggings.  The  furnace  is  a  reverberatory.  The  amount  of  ore  smelted  in 
the  district  is  not  very  large;  exactly  how  much  could  not  be  ascertained.  It  is  about 
500,000  pounds  per  annum,  or  seven  and  a  half  millions  since  1862. 


From  the  foregoing  statistics,  the  following  general  results  may  be  deduced.  There 
are  now  seven  reverberatory  or  Drummond  furnaces  in  operation,  with  an  average  daily 
capacity  of  7,000  pounds  of  ore  each;  and  five  blast  furnaces  of  two  hearths,  and  two  of 
one  hearth  each,  the  average  capacity  per  hearth  being  100  pigs,  or  10,000  pounds  of  ore 
per  24  hours.  In  addition  to  these  there  are  nine  blast  furnaces  of  two  hearths  each, 
not  at  present  worked,  but  nearly  all  in  good  repair.  Some  of  them  have  been  sup- 
planted by  the  reverberatory  furnace,  which  is  preferred  for  fine  ore,  and  some  by  new 
furnaces  built  in  adjoining  localities. 

Combining  now  the  several  amounts  of  lead  ore  already  given  as  the  product  of  the 
different  districts  for  the  several  years  since  January  1,  1862,  we  find  the  total  produc- 
tion of  the  Wisconsin  Lead  region  to  have  been  as  follows : 

Total  Product,  Total  Product, 

Year.                                               Ibs.  Year.  Ibs. 

1862 17,037,912  1870 13,754,159 

1863 15,105,577  1871 13,484,210 

1864 13,014,201  1872 11,622,668 

1865 14,337,895  1873 9,919,734 

1866 14,029,192  1874 9,625.174 

1867 13,820,784  1875 9,179,395 

1868 13,869,619  1876.  to  Oct.  1st  ....  8,747,543 

1869 13,426,721 

Total  from  January  1,  1862,  to  October  1,  1876 190,974,784 


Besides  the  smelters  already  mentioned,  there  are  numerous  others  operating  outside 
of  the  Wisconsin  Lead  region,  in  Illinois  and  Iowa.    The  following  information  was  ob- 
tained relative  to  their  production : 
The  parties  smelting  in  Dubuque  are : 

J.  &  W.  G.  Walters,  annual  amount 900,000  Bbs. 

Coates  and  Brunskill,  annual  amount 900,000  flbs. 

Fern  and  Simpson,  annual  amount 650,000  ffi>s. 

Parties  smelting  in  Galena  are: 

Thomas  B.  Hughlett,  annual  average  since  1862 ]  ,800,000  tt>s. 

Spensley's  Furnace,  present  annual  average 1,000,000  fi>s. 

Richard  Bowden,  or  Galena  Furnace,  smelted  as  follows: 

Year  1874 930,000  Ibs. 

Year  1875 850,000  Ibs. 

Year  1876,  to  October  1st 630,000  fts. 

Hon.  Henry  Green,  of  Elizabeth,  Illinois,  smelted  as  follows: 

Pounds.  Year.  Pounds. 

1873 575,113  1875 615',406 

821,720  1876,  to  October  1st ....  -142,602 


Mr.  Green  remarks  that  seven  years  ago  the  mineral  field  which  supplies  his  furnace 
produced  three  times  as  much  ore  as  at  present. 


750 


GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 


The  amounts  smelted  by  Richards  &  Co.,  at  their  furnace  in  Warren,  Illinois,  are  ap- 
pro>dmately  as  follows : 


Year. 
1873. 

1874. 


Pounds. 
450,000 
300,000 


Year.  Pounds. 

1875 250,000 

1876,  to  October  1st. . . .       200,000 


Inasmuch  as  no  detailed  statements  could  be  obtained  from  any  of  these  parties,  or 
anything  more  than  the  foregoing  approximations,  it  is  impossible  to  give  a  correct  and 
reliable  account  of  the  several  amounts  they  have  smelted  since  1862.  By  comparing 
their  present  product  with  that  of  other  parties  in  former  years,  it  is  estimated  that 
they  have  smelted,  since  January  1,  1862,  about  one  hundred  million  pounds. 

As  it  is  a  matter  of  interest  to  compare  the  present  production  of  the  mines  with  tlio 
past,  I  have  taken  the  liberty  to  reproduce  the  following  statistics  of  the  Upper  Missis- 
sippi Lead  mines,  the  product  being  given  in  tons  of  metallic  lead.1 


Price  per  cwt. 

Year. 

Tons. 

in  St.  Louis. 

1823  

150 

.... 

1824  

78 

1825  

297 

.... 

1826....:. 

428 

.... 

1827  

.  .  .  .      2,313 

$4.50 

1828  

.  .  .  .      4,958 

3.30 

1829  

.  .  .  .      5,957 

2.00 

1830  

.  .  .  .      5,331 

2.13 

1831  

.  .  .  .      5,369 

3.00 

1832  

.  .  .  .      5,401 

4.25 

1833  

.  .  .  .      6,068 

4.13 

1834  

,  .  .  .      7,699 

4.25 

1835  

.  .  .  .      8,469 

5.00 

1836  

11,390 

5.13 

1837  , 

.  .  .  .      9,708 

.  .  .  . 

1838  

..   .     10,811 

.... 

Price  per  cwt. 

Year. 

Tons. 

in  St.  Louis. 

1839  

.  .     11,976 

$4.38 

1840  

..     11,987 

4.38 

1841  

.  .     14,150 

3.50 

/ 

At  Galena, 

1842  

.  -     13,992 

$2.24 

1843  

.  .     17,477 

2.34 

1844  ....... 

.  .     19,521 

2.82 

1845  

.  .     24,328 

2.96 

1846  

.  .     23,513 

2.88 

1847  

..    24,145 

3.17 

1848  

..    21,312 

3.24 

1849  

..    19,654 

3.67 

1850  

..     17,768 

4.20 

1851  

...    14,816 

4.08 

1852  

..     12,770 

4.12 

1853  

..     13,307 

5.50 

I  am  also  indebted  to  Messrs.  N.  Corwith  &  Co.,  of  Galena,  for  the  following  con- 
densed statement  of  the  production  of  the  Upper  Mississippi  Lead  mines: 

Years.  Pigs. 9  Tons. 

1821  to  1831 664,118  23,244 

1831  to  1841 1,591,950  55,718 

1841  to  1851 6,170,857  215,979 

1851  to  1861 4,609,553  161,334 

1861  to  1871 2,419,985  84,700 

1872 200,000  7,000 

1873 200,000  7,000 

1874 150,000  5,400 

1875 150,000  5,400 

To  Oct.  1876 125,000  4,500 


1  See  Whitney's  Metallic  Wealth  of  the  United  States,  1854,  p.  421. 

2  The  weight  of  a  pig  of  lead  is  about  72  pounds. 


CONCLUDING  REMARKS.  751 


COXCLUDIXG  EEMAEKS. 

In  the  preparation  of  this  report,  I  have  been  actuated  by  many  considerations  which 
have  to  a  great  extent  determined  its  character  and  contents.  In  the  first  place,  the 
space  which  can  justly  be  devoted  to  the  Lead  region  in  a  report  on  the  entire  state  is 
necessarily  small,  and  involves  a  judicious  selection  of  the  material  collected  and  pre- 
pared. 

In  the  course  of  my  examinations  in  the  Lead  region,  I  have  found  in  all  places,  and 
among  all  persons  connected  with  the  mining  interests,  a  general  expression  of  a  desire 
for  information  in  regard  to  the  condition  of  the  mining  industry  in  those  portions  of 
the  Lead  region  more  or  less  remote  from  the  ones  in  which  they  reside.  To  furnish 
such  information  is  undoubtedly  a  legitimate  object  of  a  work  of  this  kind,  and  to  it, 
therefore,  I  have  devoted  about  two-thirds  of  this  report,  reserving  the  remainder  for 
the  geological  and  topographical  examinations  contemplated  by  the  law. 

Among  other  subjects  which  I  have  been  obliged  to  omit  is  the  much-argued  ques- 
tion of  mining  in  the  Lower  Magnesian  limestone.  No  discussion  of  thia  question  can  do 
it  justice  which  does  not  take  into  consideration  the  origin  of  the  crevices,  and  the  man- 
ner of  deposition  of  the  ores  and  associate  minerals  contained  in  the  mines  now  operated, 
since  these  questions  are  the  only  premises  from  which  we  can  derive  any  reliable  con- 
clusions. 

The  discussion  of  this  question  would  have  occupied  more  space  in  the  report  than  I 
felt  justified  in  devoting  to  theoretical  questions,  at  the  expense  of  what  appeared  to  me 
to  be  important  practical  facts. 

The  subject  of  drainage  in  our  mines  is  one  of  great  importance;  at  present  it  is  ef- 
fected by  pumping,  and  by  levels  or  adits.  Pumping  is  at  best  but  a  temporary  expe 
dient,  and  when  steam  is  employed  it  is  a  costly  one ;  it  effects  the  drainage  of  only  a 
comparatively  small  area,  and  when  the  pump  ceases  to  work,  water  immediately  returns 
Expensive  pumping  operations  are  only  warranted  where  large  bodies  of  ore  are  known 
to  exist,  within  a  small  area  of  ground. 

On  the  other  hand,  the  drainage  effected  by  a  level  is  permanent  and  extensive,  al- 
though the  original  outlay  of  capital  is  large.  Our  mines  have  now  been  worked  so  long 
that  it  is  known  in  each  mining  locality  how  many  ranges  have  been  worked  to  the  nat- 
ural water  level,  and  the  comparative  value  of  the  veins  of  ore  left  in  them  when  aban- 
doned. With  this  foreknowledge  it  is  not  difficult  to  arrange  a  level  that  will  not  only 
drain  the  previously  known  ranges,  but  will  also  make  it  possible  to  work  any  others 
which  may  afterwards  be  discovered  in  its  vicinity;  a  system  which  is  further  favored  by 
the  well  known  parallelism  of  the  ranges. 

The  stratum  in  which  levels  can  be  most  rapidly  excavated,  and  with  the  least  ex- 
pense, is  the  upper  or  thin-bedded  portion  of  the  Blue  limestone  (Trenton).  There  are 
no  interstratified  beds  of  clay  above  it,  and  usually  nothing  to  prevent  the  drainage  of 
all  the  Galena  limestone;  but  as  the  strata  sometimes  contain  slight  flexures,  it  is  not 
always  possible  to  drive  a  level  in  the  same  formation.  Levels  driven  in  this,  the  upper 
pipe-clay  opening  have  the  additional  advantage  of  proving  one  of  the  most  produc- 
tive openings  known  in  the  Lead  region. 

Judging  from  the  number  of  levels  which  have  been  excavated,  and  the  success  which 
has  usually  attended  them  when  completed,  the  system  of  mining  by  levels  seems  to 
offer  the  safest  field  for  the  employment  of  capital. 

The  recent  inventions  and  improvement  in  pneumatic,  or  compressed  air  drills,  and 
in  mining  explosives,  such  as  dynamite  and  rendrock,  are  daily  rendering  the  excava- 
tion of  levels  a  much  less  laborious  task. 


752  GEOLOGY  AND  TOPOGRAPHY  OF  THE  LEAD  REGION. 

There  is  another  method  by  which  drainage  of  mines  has  sometimes  been  effected, 
and  which  might  in  many  other  places  be  employed  to  advantage.  It  is  by  simply  drill- 
ing a  hole  from  the  bottom  of  the  mine  to  some  of  the  underlying  clay  beds  of  the 
Trenton.  In  this  way  a  passage  is  often  effected  for  the  escape  of  the  water,  of  which 
it  will  often  avail  itself  until  the  opening  becomes  closed  with  mud  from  the  mine,  when 
a  new  hole  has  to  be  drilled. 

In  many  portions  of  the  Lead  region,  but  more  especially  in  the  southern  and  centra 
parts,  there  is  a  desire  which  has  often  been  earnestly  expressed  to  me,  that  a  survey 
should  be  made  of  the  ore-bearing  ranges  both  old  and  new.  Such  a  survey,  to  be  of 
any  practical  benefit,  should  be  made  with  a  transit  and  level,  and  with  the  utmost 
accuracy.  It  should  be  made  underground  when  possible,  and  when  not,  it  should  be 
.made  on  the  surface,  locating  the  ranges  from  the  shafts.  The  survey  of  each  district 
should  be  referred  to  certain  fixed  points,  whose  location  and  elevation  should  be  accu- 
rately ascertained.  The  location  of  these  points  with  reference  to  each  other  could  at 
any  time  be  ascertained  by  triangulation  if  thought  necessary.  The  whole  should  then 
be  mapped  on  a  suitable  scale  and  published  with  the  field  notes. 

The  advantages  derived  from  such  a  survey  are  chiefly  the  following:  (1)  In  ranges 
which  are  now  worked,  it  would  be  easy  to  reproduce  on  the  surface  the  areas  worked 
out  below,  and  from  the  known  course  of  the  range  the  miner  could,  with  considerable 
certainty,  locate  his  shafts  so  as  to  reach  the  unworked  portions,  thus  effecting  a  large 
saving  of  time,  labor  and  money  wasted  in  prospecting.  (2)  The  surface  of  the  Lead 
region  is  rapidly  becoming  an  agricultural  country.  In  many  places  the  old  shafts  are 
being  filled,  the  dump  piles  are  being  removed,  and  all  surface  vestiges  of  once  val- 
uable ranges  are  becoming  obliterated.  Many  of  these  ranges  were  worked  many 
years  since  for  lead  ore  alone,  to  the  natural  water  level,  and  abandoned  with  valuable 
bodies  of  ore  still  remaining  in  them;  and  in  view  of  the  increasing  production  of  zinc 
ore,  which  is  now  between  three  and  four  times  that  of  lead  ore,  it  is  not  unlikely  that 
it  may  become  profitable  to  work  them  again.  From  a  survey  such  as  is  outlined 
above,  the  location  of  old  shafts  and  ranges  could  at  any  time  be  restored.  (3)  It  would 
conduce  to  the  systematic  working  of  the  mines  in  the  future,  by  forming  a  basis  to 
which  private  surveys  could  be  referred,  and  would  indicate  the  points  where  levels 
could  be  most  successfully  placed  for  the  drainage  of  the  mines. 

These  are  but  a  few  of  the  advantages  which  will  occur  to  persons  actually  engaged 
in  mining.  Probably  there  is  enough  money  wasted  in  prospecting  every  year,  which 
would  be  saved  by  such  a  survey,  to  carry  it  on  to  a  successful  termination. 


INDEX. 


A. 

Acknowledgments,  89,  93,  412,  651. 

Adams  County,  529,  566. 

Age  of  Milwaukee  Cement  Rock,  397. 

Agriculture,  41. 

Aimapee,  elevations,  107. 

spring,  148. 

nver,  204. 

drift,  228. 
Albion,  elevations,  435. 

Trenton  limestone,  558. 
Albite,  28. 
Amphibole,  28. 
Analysis  of  Barite,  693. 

brick,  236. 

carbonaceous  shale,  673,  680. 

cement  rock,  396. 

glass  rock,  681. 

greensand,  536. 

iron  ore,  331,  498. 

kaolin,  468,  469,  471,  476. 

limestone,  152,  282,  284,  292,  298,  309, 
338,  345,  381, 390,  393,  399,  543, 560, 
561. 

marl,  239. 

pig  iron,  332. 

soils,  196. 

St.  Peters  sandstone,  680. 

waters,  31,  146,  152,  161,  660. 
Andrews,  Dr.  E.,  96. 
Angelica,  elevations,  107. 

Lower  Magnesian  limestone,  283. 

Trenton  limestone,  303. 
Anglesite,  29,  693. 
Annual  Report  of  1873,  5. 

1874,  45. 

1875,  67. 

Ansley  Range,  741. 
Antisdel,  89. 
Apatite,  29. 
Appleton  brick,  237. 

flux  used  at,  341. 
Galena  limestone  at,  312. 
springs  at,  148. 

Archaean  formations,  general  description, 
248,  461. 

areas,  isolated,  248,  501. 
table  of  isolated  areas,  503. 
Wis.  SUR.  — 48 


Arlington,  elevations  in,  442. 
general  description,  585. 
Lower  Magnesian  limestone,  547. 
St.  Peters  sandstone,  556. 
Arrangement  of  report  of  Cent.  Wis.,  411. 
Arsenical  Nickel,  28. 
Arsenides,  28. 
Artesian  Wells,  149. 

in  Auroraville,  150-159. 
Byron,  150,  155. 
Calumet,  150,  158. 
Fond  du  Lac,  150-154. 
Green  Bay,  150. 
Janesville,  151, 166. 
Madison,  50,  533. 
Manitowoc,  150,  162. 
Milwaukee,  151,  164,  336. 
Oakfield,  150,  155. 
Oshkosh,  150,  151,  155,  158. 
Palmyra,  151,  161. 
Poysippi,  150-159. 
Racine,  151,  163. 
Rushford,  150,  159. 
Sheboygan, 151,  164. 
Taycheedah,  150,  154. 
Watertown,  150,  160. 
Whitewater,  150,  162. 
Western  Union  Junction,  151,  162, 

336. 
possibilities    of    obtaining,     at    other 

points,  167. 
Ashford,  elevations,  107. 

Niagara  limestone  in,  350,  356. 
Ashippun,  Cincinnati  shales  in,  317. 

^Niagara  limestone  in,  340,  343. 
Asphaltum,  29. 
Auburn,  elevations  in,  107. 
Aurora,  Artesian  weULs  in,  150,  159. 

cranberries  in,  186. 
Avon,  elevations  in,  107, 169. 
Aztalan,  elevations,  107. 

Trenton  limestone  in,  301. 


B. 

Bacon,  C.  S.,  93,  106. 
Baileys  Harbor,  204. 

Niagara  limestone  at,  352,  353. 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


Ballard  Range,  742. 
Bar,  691. 
Baraboo,  595. 

ranges,  427,  504,  523. 

elevations,  446. 

river,  420. 
Barite,  29,  693. 
Bark  river,  136. 
Barometrical    Observations,    106,   429, 

649. 

Barry,  Rev.  A.  C  ,  152. 
Bartholomew's  Bluff,  264,  265. 
Barton,  elevations,  107. 
Bass  Lake,  139. 
Beach  Formation,  A,  219. 

B,  224. 

C,  225. 

D,  225. 

Beach  line,  131,  226,  228. 

elevations  of,  228. 
Bear  Lake,  140. 
Beaver  Dam,  elevations,  107. 

peat  in,  244. 

springs  in,  143. 

Trenton  limestone  in,  301. 
Beetown  District,  695,  744. 
Belgium,  elevations,  107. 
Belle vue,  elevations,  107. 
Beloit,  elevations,  107. 

drift,  213,  215,  226. 

Trenton  limestone  in,   292,  297,  298, 

305. 
Berlin,  Springs,  near,  142,  149. 

red  clay  at,  223. 

peat  near,  243. 

porphyry  at,  249,  520. 

Potsdam  sandstone,  267. 
Big  Bend,  Oconto  river,  267. 
Big  Bull  Falls,  486,  494. 
Big  Foot  Prairie,  136. 
Black  Creek,  281. 
Black  lead,  27. 
Black  river,  421. 
Black  River  Falls,  493,  546,  565. 

station,  499. 

Blaney,  J.  V.  Z.,  35,  146.  . 
Blende,  Black  Jack,  28. 
Bloomfleld,  elevations,  107. 
Blue  Beds,  Upper,  291,  296. 

Lower,  291,  294. 
Blue  limestone,  291,  560,  680. 
Blue  Mounds,  661. 

Bode,  Gustavus,  analyses  by,  30,  35,  72, 
86,  88,  146,  164,  282,  309,  381,  390,  393. 
Borings  in  peat,  242-245. 
Bornite,  692. 
Bowlders,  208,  218, 618. 

of  clay,  210. 

of  gravel,  219. 
Bowlder  Clay,  217,  220. 
Bow's  Hill,  266. 
Bradford,  elevations,  107. 

Galena  limestone  in,  308. 
Brandecke,  Dr.  L.,  analysis  by,  161. 
Brick,  manufacture  of,  235,  630,  665. 

fire,  470. 
Brighton,  elevations,  107. 


Brillion,  elevations,  107. 

marble,  347. 
Bristol,  601. 

elevations,  107,  108,  441. 

Lower  Magnesian  limestone  in,  547. 
Brooks,  Maj.  T.  B.,  45,  60,  64,  72. 

survey  of  1874,  60. 
Brookfield,  elevations,  108. 
Brooklyn,  springs  in,  149. 

Lower  Magnesian  limestone,  277. 
Brown,  Rev.  W.  P., .93. 
Brown  county,  Cincinnati  shales  in,  318. 
Brown  Deer,  397,  399. 
Brown  Rock,  291,  695. 
Brown's  Lake,  140. 
Buckert's  Fountain,  161. 
Buell,  I.  M.,  93. 
Buff  limestone,  291,  560,  680. 
Buff  beds,  Upper,  291,  293. 

Lower,  291. 

Building  Stone,  249,  284,  290,  304,  303, 
337,  342, 347,  382,  383,  545, 554,  562,  6GO, 
680. 

Bull  Falls,  483. 
Burnett,  elevations  in,  108. 
Burlington,  drift,,  203,  206,  208,  211,  212. 

elevations,  108. 

Niagara  limestone  near,  372. 
Burke,  601. 

elevations  in,  439. 
Byron,  135. 

Niagara  limestone  in,  344. 

Springs  in,  148. 

Artesian  wells  in,  150,  154,  155. 
Byron  Beds,  335,  345-348,  384. 


C. 

Calcite,  29,  693. 
Calamine,  29,  693. 

district,  739. 
Calamus,  elevations,  108. 

peat,  244. 

Trenton  limestone  in,  277. 
Caledonia,  elevations,  108,  443. 

cranberries,  186. 

Lower  Magnesian  limestone  in,  277. 

Potsdam  sandstone  in,  589. 

quartzite,  504,  512. 
Calumet,_  elevations,  108. 

Artesian  wells  in,  150,  158. 
Cambria,  544. 
Carnp  Lake,  136. 
Camp  Douglas,  569. 
Canneld,  W.  H.,  412,  515. 
Canal  from  Lake  Michigan  to  Mississippi 

river,  420. 
Carltqn,  elevations,  108. 

Niagara  limestone,  378,  379. 
Carr,  E.  S.,  69. 
Cascade  Falls,  318,  333. 
Casco,  elevations,  108,  213. 

Niagara  limestone  in,  354. 
Castle  Rock,  676. 
Cedar  Creek,  136. 
Cedar  Lake,  140. 


INDEX. 


<oo 


Cedarburg,  elevations,  108. 
spring,  108,  149. 
building  stone,  383. 
Niagara  limestone  at,  362,  378,  379. 
Celestite,  29. 
Cement  Rock,  295-405 . 
Center,  elevations,  108. 

Trenton  limestone  in,  303. 
Ceuterville,  elevations,  109. 

Drift  in,  228. 

Centerville  District,  722. 
Centralia,  475,  530. 
Central  Wisconsin,  report  on,  407-639. 
District,  410. 
•Area  of,  409. 

Surface  features,  413,  424. 
River  systems,  413. 
Watersheds  of,  424. 
Former  drainage  of,  426. 
Relations  of  topography  to  geology, 

447. 

Geological  formations  of,  448. 
Drift  and  driftless  areas,  448. 
Vegetation  and  soils,  449. 
Topographical  subdivisions,  453. 
General  geological  structure  of,  457. 
Archaean  rocks  of,  461-524. 
Lower  Silurian  rocks  of,  525-607. 
Potsdam  sandstone  of,  525-547. 
Lower  Magnesian  limestone  of,  547- 

555. 

St.  Peters  sandstone  of,  555-558. 
Trenton  limestone  of,  558-562. 
Galena  limestone  of,  562. 
Local   details,   Silurian  formations, 

563,  607. 

Quaternary  deposits,  608-632. 
i\iicroscopic  lithology,  637-639. 
Cerussite.  29,  694. 
<  'halcopyrite,  28,  693. 
t'halcosi'te,  28. 
Chalybeate  Springs,  148. 
Chaiiifc^rlin,  J.  H.,  v.,  52,  93,  106. 
Chamberlin,  T.  C.,  6,  44,  46,  64,  65,  66, 
71,  85,  427,  502,  504,  506,  521,  542,  543, 
553,  557,  559,  673. 
Party  of,  1873,  8. 
Party  of,  1874,  51. 
Champlain,  219,  224. 
Chandler,  Dr.  C.  F.,  146,  165. 
Charlestown,  elevations,  109. 
Chert,  268. 
Chilton,  109,  223. 
Chimneys,  690. 
Christiana,  elevations,  170,  436. 

Trenton  limestone  in,  558. 
Cincinnati  Group,  in  Eastern  Wisconsin, 
314-326. 

in  Lead  region,  685. 

Fossils  in,  315, 320. 

Clark  County,  general,  563, 

Special  references,  461,  529,  541. 
Clay  Banks,  elevations,  109. 
Clear  Lake,  140. 
Clifton,  137. 

Brick  made  at,  238. 
Cincinnati  formation  at,  818. 


Clifton,  Niagara  limestone  at,  339. 
Clinton,  elevations,  109. 

Iron  ore  deposit,  327-335. 
Clyinan,  elevations,  109. 
Coal,  316,  317. 
Cobb,  J.M.,  171. 
Cold  Spring,  elevations,  109. 
Columbia  County,  general,  579. 

Special  references,  529,  532,  534,  547, 

558. 
Columbus,  elevations,  442. 

Lower  Magnesian  limestone  in,  547. 
St.  Peters  sandstone  in,  556. 
Como  Lake,  139. 
Comstock,  Gen.  C.  B.,  61,  104. 
Conant's  Kapids,  478,  564. 
Concord,  elevations,  109. 
Cranberries  in,  186. 
Conglomerate,  254. 
Conover,  A.  D.,  v,  9,  651. 
Cooperstown,  elevations,  109. 

Niagara  limestone,  350,  354,  383. 
Copper,  27,  210,  619. 
Carbonate,  28. 
in  Lead  Region,  741. 
Copperas,  29. 
Coral  Beds,  Upper,  335,  351,  357,  384. 

Lower,  335,  348,  351,  384. 
Coral  Reefs,  369-371. 
Cottage  Grove,  600. 
Elevations,  437. 
St.Peters  sandstone  in,  556. 
Courtland,  elevations,  444. 

Lower  Magnesian  limestone  in,  547. 
St.  Peters  sandstone  in,  556. 
Trenton  limestone  in,  558. 
Cranberries,  182,  186,  187. 
Crawford,  J.  W.  T.,  9. 
Crevice,  689. 

Cross  Plains,  elevations,  436. 
St.  Peters  sandstone  in,  556. 
Trenton  limestone  in,  559. 
Cuprite,  28. 

Current,  along  shore  of  Lake  Michigan, 
130,  132. 
iyanite,  29 


D. 

Dale,  elevations,  109. 
[)alles  of  the  Wisconsin,  570. 
[)ana,  Prof.  J.  D.,  79,  370. 
Dane,  elevations,  170,  440. 
Lower  Magnesian  in,  547. 
County,  general,  597, 
Special  references,  529,  534,  558. 
Daniells,  Prof.  W.  W.,  analyses  by,  6, 60, 

64,  72,  284,  285,  339,  345,  381,  680. 
Dajiiels,  Edward,  68,  69,  95,  647. 
Darien,  206. 

elevations,  109. 
)arlington,  681. 
)arwin,  Chas.,  370. 
Da  vies,  Prof.  J.  E.,  26,  6< 
Davis,  W.  N.,  158. 
Day,  Dr.  F.  H.,  369,  371. 


T56 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


Dayton,  Mendota  bods,  266. 
Deerfteld,  elevations,  438. 

St.  Peters  sandstone  in,  556. 

Trenton  limestone  in,  558. 
Dekorra,  elevations,  438. 
Delavan,  elevations,  109. 

Springs,  147,  149. 

Lake,  136,  139. 
Delafleld,  elevations,  105,  213. 

Springs,  31,  149. 

Cranberries,  186. 

Drift,  211. 

Niagara  limestone  in,  339,  -343. 
Delona,  elevations,  447. 
Dendritic  Markings,  550. 
De  Pere,  elevations,  109. 

Galena  limestone,  312. 

Cincinnati  shales,  318. 

Iron  ore,  near,  333. 
Devil's  Lake,  507-511. 
Devonian,  395-405. 
Diagonal  valley,  99. 
Diggings  — 

Adams  &  Bowder,  729. 

AdMnson,  698. 

Alderson,  J,  700. 

Anthony  &  Dixon,  709. 

Arthur  &  Co.,  698,  736. 

Ashworth,  E.,  712. 

Badcroft,  737. 

Brainbridge,  718. 

Brainbridge,  Mundy  &  Maighn,  718. 

Brainbridge  &  Vipond,  718. 

Bennett  <fe  Brady,  735. 

Bennett  &  Co.,  735. 

Benton  District,  717. 

Biddick,  738. 

Big  Patch,  721. 

Big  Pump,  706. 

Bininger  .Range,  706. 

Black  &  Co.,  701. 

Blackney,  Donahue  &  Co.,  723. 

Bohan  &  Co.,  735. 

British  Hollow,  700. 

Brown  Bros.  &  Parish,  696. 

Brown  &  Co.,  739. 

Brown  &  Cluthers,  737. 

Brown,  Dodge  &  Co.,  710. 

Bull  Pump  Range,  706,  717. 

Buncome,  708. 

Cain  &  Read,  738. 

Calamine,  739. 

Carpenter  &  Bennett,  708. 

Carter  &  Owens,  731. 

Carter  &  Samuels,  722. 

Catchall,  712. 

Centerville,  722. 

Champion,  710. 

Chandler's,  707. 

Clark's,  706. 

Clayton  &  Co.,  739. 

Clebenstein,  738. 

Clegg,  Samuel,  731. 

Conly  &  Sons,  738. 

Connaughton  &  Casserly,  735. 

Cox  &  Sons,  733. 

Craig,  710. 


Diggings  —  continued. 
Craig  Level  Co.,  710. 
Craig,  Sanders  &  Campbell,  710. 
Crossly,  J.  &  Co.,  696. 
Crossly  &  Bass,  696. 
Cumow  &  Pillow  Range,  700. 
Davis  &  Co.,  725. 
Dawson's,  709. 
Diamond  Grove,  738. 
Dilger,  700. 

Dodgeville  District,  730. 
Drybone,  709,  716. 
Drybone  Hollow  Range,  723. 
Duncan  Range,  720. 
Dunn  &  Son,  737. 
Dunstan  Range,  725. 
Dutch  Hollow,  701. 
Dutch  Hollow  Level  Co.,  701. 
Dutch  Lot,  711. 
Dutch  Range,  721. 
Edwards  Estate,  707. 
Edwards,  John,  706. 
Emery  &  Davis,  700. 
Eustice,  Richard  &  Co.,  706. 
Eustice,  W.  H.  &  Bro.,  707 
Evans,  Mrddeth,  731. 
Fairplay  Level  Co.,  704. 
Farwell  &  Co.,  732. 
Flynn,  Lynch  &  Co.,  724. 
Frame  &  Co.,  740. 
Furfee  &  Co.,  739. 
Garden  &  Son,  739. 
Gillilan,  Henry,  700. 
Gillis  Range,  720. 
Goldswortliy  &  Bro.,  736. 
Goldsworthy  &  Hocks,  737. 
Graham  Mining  Co.,  697. 
Grant,  699. 

Greenwood  &  Miller,  709. 
Griswold,  700. 
Hackett's,  767. 
Hall  &  Rain,  712. 
Hamilton,  740. 
Harper,  Hird  &  Co.,  711. 
Harris  &  Long,  736. 
Harris  &  Stanley,  725. 
Harvey,  718. 

Hawkins,  Thos.,  &  Co.,  721. 
Hazel  Green  Mining  Co.,  707. 
Hayward  Range,  700. 
Hendy,  Davey,  Sobey  &  Co.,  731. 
Heller  &  Parish,  722. 
Hicks,  Fiddick  &  Co.,  708. 
Highland  District,  723. 
Hinderliter  &  Sons,  723. 
Hitchins  &  Terrill,  733. 
Hoare  Bros.,  736. 
Homsnoggle  Ridge,  726. 
Howe  &  Alderson,  712. 
Hutchcroft  &  Thomas,  698. 
Hutchinson,  Dewey  &  Co.,  698. 
Huxtable  &  Son,  6a3. 
Irish,  716. 

Jacobs,  R.  S.  &  W.  J.,  729. 
Jacka  &  Waggoner,  733. 
Jackson  &  Co.,  734. 
Jeffrey  &  Bro.,  737. 


INDEX. 


Diggings  —  continued. 

Jeffrey  &  May,  737. 

Jenkins,  Miller  it  Co.,  722. 

Johns  <t  Harvey,  70S. 

Jones,  Hugh,  731. 

Jones,  Farrag-er  &  Owens,  730. 

Joseph,  H.,  738. 

Kessans,  Barney,  709. 

Kesting,  Hines  &  Co.,  709. 

Laiubly  Range,  731. 

Langstaff  &  Gillan,  701. 

Leakeley  Estate,  712 

Level  Company,  719. 

Linden  District,  726. 

Linden  Mine,  726. 

Loonn's  it  Co.,  698. 

Lost  Grove,  739. 

Lutey  &  Co.,  736. 

Maguire,  Kennedy  &  Co.,  723. 

Mankey  &  Son,  737. 

Manning  &  Delaney,  726. 

Manwaring  &  Madison  Range,  706. 

Martin  &  Cramer,  738. 

McBreen  &  Co.,  707. 

McCaffery,  Smith  &  Co.,  719. 

McCoy  Water-wheel  Range,  706. 

McDermott  &  Co.,  739. 

McElroy  Bros.,  719. 

McNulty,  714. 

Meloy  &  Fox,  716. 

Meredith,  699. 

Messersmith  Range,  720. 

Metcaif,  Harker  <fe  Alexander.  718. 

Mifflin,  721. 

Mills,  Gabriel,  708. 

Mineral  Point  District,  733. 

Mineral  Point  Mining  Co.,  735. 

ALssouri  Range,  720. 

Mitchell  &  Pollard,  734. 

Moffat  &  Co.,  707. 

Monroe,  740. 

Morrison,  D.,  729. 

Mulligan  &  Francis,  723. 

Muscalunge,  697. 

Nichols  <t  Holmes,  736. 

Nip  &  Tuck,  697. 

Oakland  Mining  Co.,  717. 

Oates  &  Eustice,  706. 

Opir  &  Lancaster,  738. 

Owens  &  Powell,  730. 

Pascoe  &  Collins,  733. 

Peak  &  Blair,  701. 

Pearce,  Jos.,  731. 

Pearce  &  Son,  739. 

Penitentiary,  721. 

Phillips  &  Walker,  699. 

Phcenix  Mining  &  Smelting  Co.,  713. 

Pierce  &  Trewather,  707. 

Pigeon,  697. 

Platteville  District,  719. 

Porter's  Grove.  732. 

Powell  &  Co.,  733. 

Poad,  Barrett  &  Tredinnick,  728. 

Prideaux  &  Henry,  736. 

Pridcaux,  Wm.,  734. 

Prisk  &  Coad,  734. 

Prisk  &  Paynter,  734. 


Diggings  —  continued. 

Purcell  &  Hardin,  740. 

Rain,  J.,  &  Co.,  712. 

Rain,  Young-  &  Jenkins,  722. 

Raspberry  Range,  712. 

Richards,  735. 

Richards  <t  Burns,  733. 

Richards  &  Faul,  729. 

Rickert,  Stephens  &  Co.,  714. 

Ridgeway  Mine,  7  •'!•_'. 

Ridgeway  Mining  Co.,  740. 

Rigger  &  Arthur,  739. 

Bitter  &  Bock,  698. 

Robarts  Range,  729. 

Robbins  &  Bros.,  712. 

Robinsons,  724. 

Robbins  Range,  720. 

Rockville,  699. 

Rogers  &  Mankey,  737. 

Ross,  J.  J.,  735. 

Rowe  &  Co.,  725. 

Rowe  &  Bowe,  706. 

Bowe  &  Vivian,  707. 

Rup  &  Son,  701. 

Schlosser  <fe  Co.,  739. 

Shepard  &  Co.,  738. 

Shields  &  Linden,  733. 

Short  &  Co.,  735. 

Short  &  Foster,  737. 

Showalter  &  Payton,  698. 

Shullsburg  District,  713. 

Siddell  &  Co.,  724. 

Silverthorn,  716. 

Simmons  &  Sons,  708. 

Sinapee,  734. 

Skinner,  Peter,  707. 
Smith  &  Anderson,  740. 
Smith  Range,  721. 
Spensley  &  Brown,  738. 
Spensley  &  Co.,  724. 
Spensley,  Winn  &  Co.,  709. 
Stone  &  Bryhon,  700. 
Stonh'ne,  713. 
Suthers  &  Co.,  736.    ' 
Swindlers  Ridge,  718. 
Tamblin,  Thos.,  729. 
Terrill  &  Badger  Ranges,  733. 
Thomas  &  Co.,  698. 
Treglowns  &  Wicks,  729. 
Thrasher  Bros.,  739. 
Trewilla  &  Strong,  737. 
Torneal,  707. 
Union  Mine,  732. 
Van  Meters  Survey,  732. 
Vivian  &  Sleep,  737. 
Warfield  Bange,  700. 
Watkia  Range,  731. 
Whig,  720. 
White  &  White,  740. 
Wilcox,  696. 

Wilkinson  &  Cronin  Range,  721. 
Williams  &  Bro.,  707. 
Williams  &  Co.,  703. 
Williams  &  Edwards,  724. 
Williams,  Evan,  730. 
Williams,  M.  J.  &  Co.,  719. 
Wiota,  740. 


758 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


Diggings  —  continued. 

Wcegler&  Co.,  735. 

Yellowstone,  739. 

Ziig,  701. 
Districts,  Eastern  Wisconsin,  94. 

Central  Wisconsin,  409. 

Lead  region,  645,  689. 
Dodge  county,  143,  170,  271. 

drift  in,  203,  215. 

St  Peters  sandstone,  286,  287. 

iron  ore,  328. 

Dodgeville  district,  730,  748. 
Dolomite  (see  Limestone),  29,  339,  693. 
Domes  of  rock,  202. 
Door  county,  225,  368. 
Dorward's  Glen,  511. 
Dover,  elevations,  109. 
Drainage,  Eastern  Wis.,  128. 

Central  Wis.,  413. 

Lead  region,  652. 

Changes  in,  174,  657. 
Drift,  Eastern  Wis.,  199-239. 

Central  Wis.,  608-632. 

Lead  region,  665. 
Driftless  region,  608,  632,  665. 
Drift  soils,  189. 
Duck  Creek,  building  stone,  308. 

Galena  limestone,  312. 
Dunes,  233. 
Dunkirk,  elevations,  434. 

Lower  Magneeian  limestone  in,  548. 

Trenton  limestone  in,  558. 
Dunn,  elevations,  436. 

Lower  Magnesian  limestone  in,  548. 

E. 

Eagle,  elevations,  109. 

cranberries,  186. 

drift,  209T211-212. 

Cincinnati  shale,  316. 

Niagara  limestone,  340,  342. 
East  Troy,  elevations,  109. 

Castleman's  quarry,  203,  359. 
Eastern  Wisconsin  district,  91. 

Acknowledgments,  93. 

Extent  of  district,  94. 

Previous  publications  relating  to  the 
region,  95. 

Topography,  97. 

Elevations,  106. 

Hydrology,  drainage,  128. 

Origin    and    geological    relations    of 
lakes,  137. 

Water  supply,  141 . 

Artesian  welts,  149. 

Water  power,  171. 

Changes  in  drainage,  174. 

Native  vegetation,  176. 

Soils,  188. 

Quaternary  formations,  drift,  199. 

Glacial  drift,  Kettle  Range,  205. 

Bowlder  Clay  or  Till,  217. 

Modified  drift,  Champlain,  Beach  For- 
mation A.,  219. 

The  Lower  Red  Clay,  221. 

Beach  Formation  B.,  224. 


Eastern  Wisconsin  district  —  continued. 
Upper  Red  Clay,  225. 

Beach  Formations  C.  and  D.,  and  Mod- 
ified Red  Clay,  225. 

Terraces,  228. 

Lake  encroachinent»  230. 

Dunes,  233. 

Erosion  and  deposit  in  progress,  233. 

Industrial  value  of  drift,  234, 

Brick,  235. 

Shell  marl,  239. 

Peat,  240. 

Table  of  formations,  247. 

Archaean  formations,  248-256. 

Lower  Silurian.    Potsdam  sandstone, 
257-267. 

Lower  Magnesian  limestone,  268-285. 

St.  Peters  sandstone,  285-290, 

Trenton  b'mestone,  290-305 

Galena  limestone,  305-314. 

Cincinnati  shales  and  limestone,  314, 
326. 

Upper  Silurian.   Clinton  iron  ore,  327, 
ooo. 

Niagara  limestone,  335-389. 

Lower  Helderberg,  390-394. 

Hamilton  cement  rock,  395-405. 
Eaton,  elevations,  109. 
Eaton,  Prof.  J.  II.,  49,  412,  504,  594. 
Eau  Claire  river,  486. 
Economic  considerations,  drift,  234-630. 

Archaean  formations,  465. 

Potsdam,  545. 

Lower  Magnesian  limestone,  284,  554. 

St.  Peters  sandstone,  290. 

Trenton  limestone,  304,  652,  683. 

Galena  limestone,  307,  683. 

Cincinnati  shales,  316. 

Clinton  iron  ore,  327. 

Mayville  beds,  340. 

Lower  coral  beds,  349. 

Waukesha,  Racine  and  Guelph  beds, 
380. 

Lower  Helderberg,  394. 

Hamilton  cement  rock,  400-405. 
Eden,  elevations,  109. 

Niagara  limestone  in,  344-346. 
Edgerton,  338. 
Edgerton,  B.  H.,  survey,  14. 
Egg  Harbor,  204, 228. 

elevations,  109,  229. 
Elevations,  Eastern  Wisconsin,  106. 

Central  Wisconsin,  428. 

Lead  region,  650. 

Oconto  county,  14. 

of  lakes,  23, 24. 

of  summits,  24. 

of  beach  ridges,  228,  229. 

of  junction  St.  Peters  and  Trenton,  169 

R.  R    16-23. 

Madison  to  Elroy,  429. 

Elroy  to  Merrillon,  430. 

Waterloo  to  Madison,  430. 

Edgerton  to  Black  Earth,  430. 

Camp  Douglas  to  Randolph,  431. 

Toinah  to  Wausau,  431. 

Amherst  to  Merrillon,  432. 


INDEX. 


759 


Elevations  —  continued. 

Portage  to  Stevens  Point,  433. 

Stevens  Point  to  N.  line  of  township, 

29,  433. 
Elba,  elevations,  109,  170. 

Lower  Magnesian  limestone  in,  472. 

Trenton  limestone,  301. 
Elizabeth  Lake,  139. 
Elkhart  Lake,  140. 
Elkhorn,  212. 
Ellington,  springs,  149. 

Lower  Magnesian  limestone,  230. 
Emmet,  elevations,  110. 
Empire,  elevations,  110. 

springs,  148-149. 

Niagara  limestone  in,  344,  346. 
Encroachment,  Lake,  230. 
End,  Hon.  George,  164. 
Epidote,  28 

Erin,  elevations,  110,  213. 
Erosion  in  progress,  233. 
Eureka,  276. 
Excelsior,  elevations,  447. 

quartzite,  504. 


F. 


Fairfleld,  elevations,  447. 
Fairchild,  Gov.  L.,  71. 
Fairplay  district,  701. 
Farmington,  elevations,  110. 
Fault,  280,  289,  332. 
Featherstonhaugh,  G.  W.,  67,  95. 
Feldspar,  28. 
Fertilizer,  peat  as,  245. 

shell  marl,  239. 

Fiord  features,  202,  204,  205. 
Fire  brick,  470. 
Fish  creek,  204,  228,  229. 
Fish  remains,  396. 
Fisher,  Prof.  Davenport,  49. 
Fitchburgh,  elevations,  435. 

St.  Peters  sandstone  in,  556. 

Trenton  limestone  in,  558. 
Flintville,  Galena  limestone  at,  313. 
Fluvial  pairs,  136. 
Flux,  332,  338,  341,  365,  383,  562. 
Fond  du  Lac  county,  143,  170,  206. 

Artesian  wells  at,  150.  151. 

Galena  limestone  at,  310. 

Niagara  limestone  near,  346. 

Building  stone  near,  343. 
Forests,  177,  175,  449,  660. 

removal  of,  175. 
Forrest,  elevations,  110. 
Forrestville,  elevations,  110. 

Niagara  limestone  in,  352,  354. 
Formations  of  Eastern  Wisconsin,  247. 

Central  Wisconsin,  460. 

Lead  region,  668. 
Fort  Winnebago,  585. 

elevation,  444. 
Fossils  of  drift  material,  209,  210,  213. 

of  Potsdam,  245,  261,  262,  670. 

of  Lower  Magnesian,  271,  276,  283, 554, 
675. 


Fossils  —  continued. 

of  St.  Peters,  288,  558. 

of  Trenton,  292,  294,  296,  299,  320,  561. 

of  Galena,  307,  314,  320,  685. 

of  Cincinnati,  315,  316,  320. 

of  Mayville  beds,  339,  340. 

of  Byron  beds,  346. 

of  Lower  coral  beds,  349. 

of  Upper  coral  beds,  351,  353. 

of  Waukesha  beds,  358,  359. 

of  Racine  beds,  372,  377. 

of  Guelph  beds,  379,  380. 

of  Niagara  group,  384. 

of  Lower  Helderberg,  392,  393. 

of  Hamilton,  396,  399,  400. 
Foye,  Prof.  J.  C.,  172. 
Fox  Lake,  elevations,  110,  170. 

Trenton  limestone  in,  301. 

Galena  limestone  in,  310. 
Fox  River,  100,  420,  422,  423. 

elevations  of,  424. 

Illinois,  129. 
Fountain,  568. 
Fountain  prairie,  elevations,  443. 

Lower  Magnesian  in,  547. 
Fountains.    See  Artesian. 
Franklin,  elevations,  110,  111,  445. 
Freedom,  elevations,  446. 

Quartzite  in,  504,  518. 
Fredonia,  elevations,  111. 

Milwaukee  river  in,  131. 

Lower  Helderberg  in,  392-394. 
Fort  Atkinson,  Trenton,  301. 

Galena  limestone  in,  309. 

lime,  308. 
Fuel,  peat  as,  245. 
Fulton,  elevations,  111,  169. 

Trenton  limestone  in,  300. 
Furnaces,  iron,  332. 

lead,  749. 


G. 

Galena  limestone  in  Eastern  Wis.,  305. 

in  Central  Wis.,  562,  562. 

in  the  Lead  Region,  683. 
Galenite,  28,  554,  672. 
Garnet,  28. 

Garrison,  C.  B.,  land  of,  476. 
Gault,  J.  C.,  162. 
Geikie,  Prof.,  208. 
Geodetic  survey,  25,  62. 
Geology  of  Eastern  Wisconsin,  91. 

of  Central  Wisconsin,  407. 

of  Lead  Region,  643. 
Geological  relations  of  lakes  of  East- 
ern Wisconsin,  137. 
Genesee,  elevations,  111. 

Niagara  limestone  in,  359,  383. 

lime,  383. 
Geneva  Lake,  136-139. 
Germantown,  elevations,  111. 

Niagara  limestone  in,  363,  364. 
Gibson,  elevations,  112. 

Niagara  limestone  in,  352,  354. 
Gibralter  Bluff,  587. 


T60 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


Gillette,  elevations,  112. 

Gillet,  E.  J.,  153. 

Gillmore,  Gen.  Q.  A.,  283,  401,  405. 

Glacial  drift,  205,  630,  665. 

features,  98,  130,  131,  137, 139,  199. 

lakes,  139. 

movements,  199. 

striae,  200,  201,  205,  625. 
Glass  rock,  291,  695. 
Glass  sand,  290,  558,  546. 
Glauconite,  29,  259,  261,  536. 
Gneiss  (see  Archcean  rocks),  463,  501. 
Gold,  27,  466. 
Gouge,  691. 

Government  surveys,  24. 
Grafton,  elevations,  112. 

Niagara  limestone  in,  362,  372,  377, 

379. 

Grand  Chute,  springs,  148. 
Granite  (see  Archaean  formations),  248, 
463,  501,  521. 

intrusive,  463. 

Marion,  552. 

Mukwa,  248. 
Grand  Rapids,  133,  284,  471,  477,  530, 

546,  564. 
Granville,  elevations,  112. 

Niagara  limestone  in,  365,  377,  379. 

Lower  Helderberg  limestone,  391. 

Hamilton  cement  rock,  339. 
Grant  river,  656. 
Graphite,  27. 
Gray.  Hon.  H.  H.,  742. 
Green  Bay,  137,  318,  334. 

elevations,  113. 

Artesian  wells,  150. 

peninsula,  201,  202,  204, 342,  346,  363. 

valley,  99,  129,  199,  200-202,  223. 

valley,  cause  of,  101. 

river  system,  129,  132. 
Green  Lake,  138,  139,  266,  529. 

county,  578. 

county,  drift  in,  217. 

Potsdam  sandstone  in,  264. 

Lower  Magnesian  limestone  in,  272. 

St.  Peters  sandstone  in,  289. 

Trenton  limestone  in,  301. 
Green  Rock,  291,  695. 
Greenbush,  elevations,  113. 

drift  in,  211. 
Greenfield,  elevations,  113,  446. 

Niagara  limestone  in,  362,  369,  372. 

lime,  382. 

quartzite,  504. 

general  description,  594. ' 
Guelph  limestone,  335,  377-383,  384. 
Gypsum,  29,  315,  319. 


H. 

Hackett's  district,  659. 

Hagerman,  J.  JM  470. 

Hall,  Prof.  J.,  69,  95,  351,  411,  504,  527, 

528,  545,  559,  649,  687. 
Hamilton  cement  rock,  395,  405. 
Hamilton,  or  Lower  Helderberg?,  79. 


Hampden,  Lower  Magnesian  limestone  in, 

547. 

St.  Peters  sandstone  in,  556. 
Trenton  limestone  in,  558. 
Harmony,  elevations,  114. 
Hartford,  elevations,  114,  213. 
springs  in,  149. 
Cincinnati  shales  in,  317. 
iron  ore  in,  332. 
Niagara  limestone  in,  340,  343. 
Haven,  Geo.,  55,  65. 
Hebron,  elevations,  114; 

cranberries,  186. 
Helderberg,  Lower,  79,  390. 
Hematite,  28,  329,  693. 
Henry,  W.  T.,  680. 
Herman,  elevations,  114. 
springs  in,  148,  149. 
drift  in,  215. 

Cincinnati  shales  in,  318. 
Highland  district,  723,  749. 
Hiner,  Hon.  W.  H.,  153. 
History  of  previous  surveys,  67. 
Hitt,  H.  D.,  155. 
Hogsbacks,  207. 
Holden's  Lake,  139. 
Holland,  elevations,  114. 
Honey  Creek  (Walworth  county),  129. 
(Sauk  county),  591. 
elevations,  446. 
quartzite,  518,  504. 
Potsdam  sandstone,  532,  534. 
Lower  Magnesian  limestone,  552. 
Hood,  G.  R.,  328. 
Horicon  marsh,  peat,  343. 

Niagara  limestone  near,  344. 
Hornblende  (see  Archaean  rocks  in  text) 

28. 
Hortonia  springs,  142,  148,  149. 

Lower  Magnesian  limestone,  277. 
Hoy,  Dr.  P.  R.,  96,  130,  163,  234,  321. 
Hoyt,  Dr.  J.  AV.,  96. 
Hovey,  W.  A.,  594. 
Hubbard  springs,  149. 

iron  ore,  328. 
Hubbs,  Rev.  G.  S.,  253. 
Humphreys,  Gen.  A.  A.,  61. 
Hunt,  Dr.  H.,  136. 
Hunt,  Dr.  T.  S.,  535. 
Hunter,  Geo.,  fountain  of,  151. 
Huronian,  251,  465. 
Hutchinson,  K.  M.,  156. 
Hutchinson,  Hon.  C.,  744. 
Hydraulic  lime,  284,  285,  305,  341,  400 

670. 

Hydrocarbon  compounds,  29. 
Hydrology,  128. 
Hydrozincite,  28. 

I. 

Industrial  value,  see  Economic  consid- 
erations. 
Introduction  to  report  of  Central  Wis., 

409 

Eastern  Wis.,  93. 
Lead  region,  645. 


INDEX. 


Intrusive  granite,  463. 
Iron,  27. 

Carbonate,  29. 

Ore,  28,  327,  3:34,  498,  546. 

Sand,  222,  239. 

Sulphate,  29. 

Ironton,  Potsdam  sandstone,  532. 
Irving.  R.  I).,  6,  44,  46,  64,  66,  71,  206 
260,  261,  332. 

Party  of  1873,  7. 

Party  of  1874.  46. 

On  Central  Wis.,  407. 
Isolated  ridges,  428. 

Arcnteaji  areas,  501. 
Ives,  Frank,  survey  of,  63. 


J. 

Jackson.  114.  115. 

County,  461,  529,  541.  563. 
Jacksonport,  elevations,  115. 

Niagara  limestone  near,  354. 
Janesville,  elevations,  115. 

Artesian  well  at,  151,  166. 

Trenton  limestone  a.t,  300. 
Jefferson,  elevations,  115. 

County,  140,  143,  170,  215,  271. 

Galena  limestone  in,  309. 
Jenney,  F.  B.,  7. 
Johnson,  J.  H.,  156. 
Johnson,  Prof.  S.  W.,  197,  245. 
Johnstown.  115. 
Jordan,  181. 
Junction  City,  481,  482. 
Juneau  county,  5'29,  533,  566. 


K. 

Kaolin,  466,  467,  468,  469,  470,  471,  476. 
Kankauna,  building  stone,  308. 

Galena  limestone  at.  312. 
Kendai  Range,  741. 
Kenosha  County,  130,  139,  163,  211. 
Kettle  Range,  105, 200, 201, 205,  615,  630. 

material  of,  208-210,  618. 

structure,  210. 

relative  abruptness  of  sides,  211, 

general  relationship,  212. 

summit  altitudes,  213. 

origin,  210-214,  630. 
Ketlles,  206,  214. 
Kewaunee,  elevations,  115. 

brick,  237. 

Niagara  limestone  in,  352,  354,  368, 
372. 

County,  211,  225. 
Kewaskum,  elevations,  115. 

Niagara  limestone  in,  350.  356. 
Kennicott,  Robert,  96. 
King,  F.  H.,  8,  53,  55,  66,  93,  318. 
Kingston,  Potsdam  sandstone,  264. 
Knapp,  Capt.,  89. 

Knight,  S.  Q.,  231 

Knobs,  676. 

Knowledge,  Importance  of  Geological,  13. 


Knowlton,  482,  483.  530. 
Koslikonong,  elevations,  115. 

Lake,  138. 

Trenton  limestone  in,  300. 
Kossuth,  115. 


L. 

La  Grange,  316. 

Springs  in,  148. 

Drift,  211. 
Labradorite,  28. 
Lake,  Town  of,  115. 

Bear,  140. 

Bass,  139. 

Brown,  140. 

Buffalo,  423. 

Cedar,  140. 

Camp,  139. 

Clear,  140. 

Conio,  139. 

Delavan,  13,). 

Devils,  507. 

Elkhart,  140. 

Elizabeth,  139. 

Geneva,  139,  141. 

Green,  139,  141. 

Holdens,  139. 

Horicon,  137. 

Koshkonong,  138,  141. 

Long,  140. 

Mary.  139. 

Michigan,  104,  137,  140. 

MuskegOj  1:34. 

Oconomowoc  cluster,  140. 

Pewaukee,  140. 

Pleasant,  139. 

Pigeon, 140. 

Poygan,  137. 

Puckawa,  138,  140. 

Round,  140. 

Rush,  138. 

Silver,  139,  140. 

Shawano,  139. 

Troy,  139. 

Turtle,  139. 

Wilke,  140. 

Winnebago,  137,  140. 

Wind,  140. 

Origin  of,  137. 

Geological  relations  of,  137. 

Encroachment,  2oO. 

Michigan  Valley,  104,  137. 
elevation  of,  104. 
system,  129,  132. 
Lake  Mills,  elevations,  116,  170. 

Springs,  148. 

Cranberries,  186. 

Peat,  244. 
[jamartine,  154. 
La  Prairie,  116. 

Lapham,  Dr.  I.  A.,  5,  44,  45,  71,  95,  108, 
130,  145,  156,  161,  231,  257,  400,  470, 
498,  619,  655. 

Report  of,  1873,  5. 

Report  of,  1874,  45. 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


Lapham,  Chas.,  106. 

S.  G.,  3,  470. 
Lapham's  Peak,  213. 
Lathrop,  Rev.  S.  E.,  93. 
Latitude  and  Longitude,  61. 
Laumonite,  29. 
Lanrentian,  465. 
Law  of  Survey,  5. 
La  Valle,  Potsdam  sandstone,  532. 
Lead,  Carbonate,  29. 

Ore,  statistics,  743. 

Reg-ion,  689. 
Lead  Region,  report  on,  643. 

Introductory  and  historical,  645. 

Elevations,  650. 

Topography,  652. 

Drainage,  652. 

Springs  and  wells,  658. 

Prairie  and  forest,  660. 

Mounds,  661.  _ 

Soil  and  subsoil,  663. 

Peat,  664. 

Brick  clav,  665.  • 

Glacial  drift,  665. 

Geological  formations,  668. 

Potsdam  sandstone,  668. 

Lower  Magnesian  limestone,  671. 

St.  Peters  sandstone,  675. 

Trenton  (Blue  and  Buff)  limestone,  680. 

Galena  limestone,  683. 

Cincinnati  group,  685. 

The  Lead  Region,  689. 

Mining  terms  defined,  689. 

Mineralogy,  691. 

Present  condition  of  mines,  695. 

Beetown  district,  695,  744. 

Potosi  district,  699,  745. 

Fairplay  district,  701. 

Hazel  Green  district,  704. 

New  Diggings  district,  710,  746. 

Shullsburg  district,  713,  747. 

Benton  district,  717. 

Platteville  district,  719,  744. 

Mifflin  district,  721. 

Centerville  district,  722. 

Highland  district,  723,  749. 

Linden  district,  726. 

Dodgeville,  730,  748. 

Mineral  Point  district,  733,  747. 

Calainine  district,  739. 

Wiota  district,  740. 

Monroe  district,  740._ 

Copper  in  Lead  Region,  741. 

Statistics  of  zinc  ore,  742. 
of  lead  ore,  744. 

Concluding  remarks,  751. 
Leadhillite,  29. 
Lebanon,  317. 
Ledge,  The,  318. 

Leeds,  Lower  Magnesian  limestone  in,  547. 
Lemonweir  river,  418. 
Lesser,  281. 
Lewiston,  444. 
Life.    See  Fossils. 
Lima,  116. 
Lime,  284,  305,  308,  341,  347,  380,  382, 

554. 


Limestone,  Mendota,  260,  535,  542. 

Lower  Magnesian,  268,  547,  671. 

Trenton,  290,  558,  680. 

Galena,  305,  562,  683. 

Niagara,  335,  686. 

Lower  Helderberg,  390* 

Hamilton,  395. 
Limonite,  28. 
Lincoln,  116. 
Lindina,  568. 

Linden  District,  mining,  726. 
Linear  topography.  612,  626. 
Linn,  116,  213. 
Lisbon,  259,  367. 
Lithographic  stone,  348. 
Lithography,  microscopical,  637. 
Lithological    characters,    given    under 

each  formation. 
Little  Green  Lake,  273. 
Little  river,  134. 

Little  Sturgeon  Bay,  Cincinnati  shales, 
314,  319. 

Iron  ore  near,  334. 

Niagara  limestone,  344. 
Little  Snamico,  116. 
Lode,  690. 

Logan,  Sir  AV.  E.,  81. 
Lodi,  586. 

elevations-,  442. 

Potsdam  sandstone  in,  544. 

Lower  Magnesian  limestone,  547. 
Lomira,  135. 
Long  Lake,  140. 

Lower  Helderberg  limestone,  390. 
Lower  Magnesian  limestone. 

Eastern  Wisconsin,  268. 

Central  Wisconsin,  547. 

Lead  Region,  671. 
Lowell,  elevations,  116,  170. 

Trenton  limestone  in,  301. 
Lowville,  elevations,  443. 

Lower  Magnesian  limestone  in,  547. 
Lucas  Point,  260. 
Lynden,  117,  223. 
Lyndon.  570. 
Lyons,  il7. 


M. 

Macadamizing,  394. 

Mackford,  Lower  Magnesian  in,  272. 

Trenton  limestone  in,  301. 
Madison,  532,  533,  543,  604. 

Elevations,  437. 

Sandstone,  260,  53-5,  542. 
Magnesian  limestone.    (See  Limestone.) 

Lower,  in  Central  Wisconsin,  547. 
Eastern  Wisconsin,  268 
Lead  Region,  671. 
Magnetic  irou  sand,  239. 
Magnetite,  21,  222,  239,  493,  520. 
Magnolia,  elevations,  117,  169. 

St.  Peters  sandstone  in,  289. 

Trenton  limestone  in,  289. 
Malachite,  29,  694. 
Manganese,  28,  693. 


INDEX. 


763 


Manitowoc,  elevations,  117. 
Artesian  wells,  150,  162. 
Brick,  2:37. 

County,  206,  210,  211,  223,  225,  283. 
Manitowoc  Rapids,  117. 
3Iaple  Grove,  117. 
Maple  Valley,  117. 
Mapleworks,  565. 
Marathon  City,  490. 
Maps,  list,  report  of  1873,  44,  64. 

1874,  64. 
Marble,  347. 
Marcellon,  elevations,  444. 

Quartz-porphyry,  519. 
Marcasite,  28,  692. 
Marinette,  cranberries,  186. 

Galena  limestone  in,  313. 
Markesan,  217. 
3Iarion,  granite,  522. 
Marl,  239. 
Marsh,  E.  S.,  34. 
Marshes,  181,  240,  450. 
Marsh  Vegetation,  181. 
Marshfleld,  117,  223. 
Marquette  County,  578.  529.  541. 

Quartz-porphyry,  251,  520. 
Mary  Lake,  139. 
Mayville  Beds,  335,  336,  345,  384. 

Mines,  328,  329,  334. 
Manston,  539. 
McChesney,  J.  H.,  95. 
Medina,  elevations,  170,  439. 

St.  Peters  sandstone  in,  556. 

Trenton  limestone  in,  558. 
Melanterite,  29. 
Meraee,  118,  213,  223. 
Menacoanite,  28. 
Menasha,  137. 

Elevations,  118. 

Brick,  238. 

Trenton  limestone  in,  302. 

Galena  limestone  in,  311. 
Mendota  limestone,  260,  535,  542. 
Menomonee,  elevations,  118. 

River,  132,  132. 

Lower  Magnesian  in,  284. 
Menomonee  Falls,  elevations,  118. 

Niagara  fossils,  372. 
3Iequon,  118. 
Merrimac,  590. 

Elevations,  446. 

Quartzite,  504. 
Merrillon,  531. 
Merriman,  G.  L.,  8,  93. 
Merton,  118. 
Meteorology,  131. 
Metomen,  128. 

Elevations,  118,  170. 
Mica,  28. 

See  also  descriptions  of  Archaean  for- 
mations. 

Microscopic  Lithology,  637 
Michicott,  118. 
Middleton,  603. 

Elevations,  437. 

Quartzite,  504. 
Mifflin  mining  district,  721. 


Milford,  118,  170. 

Milton,  118. 

Milwaukee,  elevations,  118,  119. 

River,  130. 

Artesian  wells,  151-164. 

Drift,  220,  222,  228. 

Lake  encroachment,  232. 

Brick,  237. 

Niagara  limestone,  365-372. 

Lower  Helderberg,  390. 

Cement  rock,  395-405. 
Minerals,  catalogue  of  127. 

of  Lead  Region,  691. 

Paragenesis  of,  691. 

in  St.  Peters,  679. 

in  Trenton,  683. 

Waters,  30-31,88,  146. 

Springs,  146. 
Mineral  Point,  733,  747. 
Miner,  Cyrus,  166. 
Mitchell,  119,  213. 
Montello  Granite,  521-523. 
31onroe  District,  740. 
Montrose,  elevations,  434. 

St.  Peters  sandstone,  556. 

Trenton  limestone,  558. 
Montpelier,  119. 
3Iorames,  199,  205-217,  630. 

Ground,  218. 
Moraine  Lakes,  139. 
Morrison,  119. 
Mosel,  119. 
Mosinee,  483,  484. 
Mounds,  Lead  Region,  661. 
Moundville,  Quartz-porphyry,  520,  523, 
Mount  Pleasant,  119. 
Movements,  of  drift  agencies,  199,  229. 
Mt  Maria,  266. 
Mt.  Tom,  277. 
Mud  Cracks,  276,  319,  345. 
Mud  Creek,  Quarries,  390. 
Mukwonago,  119. 
Mundig,  28. 
Munro,  J.,  7. 
Murrish,  J.,  71,  647. 
Muscalunge,  district,  695. 
Muskego,  elevations,  119. 

Granite,  248. 

Lower  Magnesian  limestone,  277,  279. 

Lake,  140. 
Musquito  Hill,  280. 

Mountain,  564. 


Narrows,  of  Baraboo  river,  lower,  513. 

of  Baraboo  river,  upper,  515. 

of  Narrow  Creek,  577. 
tfecedah,  quartzite,  523. 
Neillsville,  531,  550,  565. 
Neenah,  brick,  238. 

Trenton  limestone  near,  302. 

Galena  limestone  near,  311. 
Newark,  119,  120. 
New  Berlin,  120. 
Newbury,  131. 


76J: 


GEOLOGICAL  SURVEY  OP  WISCONSIN. 


Newbury,  Prof.  J.  S.,  81,  396. 

New  Cassel,  350. 

New  Denmark,  120. 

New  Diggings  district,  710,  746. 

New  Holstein,  120. 

New  London,  142,  280. 

New  Lisbon,  568. 

Newton,  120. 

Niagara  Limestone  in  eastern  Wis.,  335 

in  Lead  Region,  686. 
Niccolite,  28. 

Nip-and-Tuck  district,  695. 
Norway,  120. 


O. 

Oak  Creek,  120,  121. 

Oak  Grove,  121. 

Oakfield,  Artesian  Wells,  150. 

Niagara  limestone  in,  344,  346,  347. 
Oakland,  elevations,  121,  170. 

Cranberries,  186. 

Trenton  limestone  in,  301. 
Observatory  Hill,  Quartz-porphyry,  519, 
Oconomowoc,  elevations,  121. 

River,  136, 

Lakes,  140. 

Cranberries,  186. 
O'Connor,  C.,  151. 
Oconto  County,  Brook's  survey,  60. 

River,  132,  133. 

Lower  Magnesian  limestone  in,  271. 
Oconto  Palls,  281,  285. 
Oolitic  Structure,  269,  550. 
Openings,  definition,  327,  690. 
Oregon,  elevations,  434. 

St.  Peters  sandstone  in,  556. 

Trenton  limestone,  558. 
Ores,  6T9,  683. 
Organization,  6. 
Orthoclase,  28. 

See  also  descriptions  of  Archfean  rock. 
Organic  Remains,  see  Fossils. 
Origin,  of  Lakes,  138. 

of  Kettle  Range,  213. 

of  Kettles,  214. 
Osceola,  121. 
Oshkosh,  Artesian  Wells,  150,  151,  156. 

Building  Stone,  308. 

Galena  limestone,  310. 
Ottawa,  145,  316. 

Springs,  149. 

Cranberries,  186. 

Drift,  211. 

Niagara  limestone  in,  342. 
Otter  Lake,  139. 
Otsego,  584. 

elevations,  443. 

Lower  Magnesian  limestone,  547. 
Outagamie  County  — 

Potsdam  sandstone  in,  264. 

Lower  Magnesian  limestone  in,  271. 
Owen,  Dr.  D.  D..  68,  95,  '268,  410,  527-528, 

535,  502,  647. 
Oxygen  Compounds,  28. 
Ozaukee,  see  Port  Washington. 


P. 

Packwaukee,  548,  579. 
Paint  Works,  Blue  river,  722. 
Palmyra,  316. 

elevations,  121,  213. 

Artesian  well,  151,  161. 

drift,  209,  211. 

springs,  31,  145,  147. 
Paleontology  (see  Fossils). 
Paris,  121.    * 
Part  I,  Annual  reports,  1. 
Part  II,  Eastern  Wisconsin,  91. 
Part  III,  Central  Wisconsin,  407. 
Part  IV,  Lead  region,  643. 
Passage  beds,  see  Transition. 
Peat,  29,  240,  664. 
Peninsula,  see  Green  Bay. 
Pentenwell  Bock,  572. 
Pensaukee,  elevations,  121,  122. 

Galena  limestone,  near,  313. 
Percival.  J.  G.,  68,  95,  250.  410,  504,  523, 

528,  542,  647. 
Peshtigo,  river,  132,  134. 

Cranberries,  186. 

Potsdam  sandstone  on,  267. 

Lower  Magnesian  limestone  on,  283. 

Trenton  limestone  on,  303. 
Petroleum,  29. 
Pewaukee,  elevations,  122. 

lake,  140. 

striae,  glacial,  200. 

Cincinnati  shale,  317. 

beds  (Waukesha),  at,  346. 

Niagara  limestone  in,  358. 

lime,  381. 

Pecatonica  river,  655. 
Phlogopite,  28. 
Pierce,  elevations,  122. 

Niagara  limestone  in,  354. 
Pigeon  Lake,  140. 
Pike  River,  130. 
Pilot  Knob,  576. 
Pine  Bluff,  250,  520. 
Pine  Knob,  677. 
Pipeclay,  opening,  695. 
Pipeclay,  691. 
Pitts  Mill,  491. 

Platteville,  mining  district,  719,  744. 
Platte  River,  656. 
Platte  Mounds,  661,  686. 
Pleasant  Lake,  139. 
Pleasant  Prairie,  122. 
Pleasant  Springs,  600. 

elevations,  436. 

Lower  Magnesian  limestone  in,  548. 

Trenton  limestone  in,  558. 
Plover,  481. 
Plumbago,  27. 
Plymouth,  568. 

elevations  (Sheboygan  countv),  122. 

drift,  211. 
Pockets.  690. 
Polk,  122. 

Poinpey's  Pillar,  677. 
Porphyry,  249,  250,  251,  519-521. 
Portage  County,  461,  529,  541,  563. 


INDEX. 


765 


Port  Edward,  468. 

Port  Washington,  brick,  237. 

springs.  149. 

drift,  223,  228. 

lime,  381. 

Ports  de  Morts,  353. 
Porter,  122.  163. 
Portland,  elevations,  122. 

drift,  202,  214. 

quartzite,  252,  256. 

Trenton  limestone  in,  301. 
Post- Glacial  features,  98. 
"  Pots  and  Kettles,"  206. 
Potholes,  206. 

Potosi  district,  699,  745. 
Potash  Kettle  Range,  205. 
Pottery,  239. 

Potsdam  sandstone,  in  Eastern  Wiscon- 
sin, 257-267;  in  Central  Wisconsin, 
525;  in  Lead  region,  668. 
Powers,  L.  N.,  469. 
Poygan,  Lake,  137. 

Lower  Magnesian  in,  277. 

lime,  285. 

Prairies,  177,  184.  449,  660. 
Prairie  du  Sac,  591. 

elevations,  445. 
Preble,  122,  123. 
Pre-glacial  features,  97. 
Prehnite,  29. 

Previous  publications,  95,  527,  647. 
Primrose,  elevations,  434. 

Trenton  limestone  in,  559. 
Puckawa  Lake,  138. 
Pyrite,  28,  692. 


Q. 

Quartz,  28. 

See  also  descriptions  of  Archaean  rocks. 
Qnartzite,  Portland  and  Waterloo,  252, 
256. 

Baraboo,  504,  519. 

Necedah,  52:  >. 

Rib  Hill,  485. 

Quartz-Porphyry,  249,  251,  519,521. 
Quaternary  formations,    Eastern   Wis- 
consin, 199. 

Central  Wisconsin,  608. 

Lead  Region,  665. 

E. 

Robbins,  Mr.,  land,  477. 
Racine  county,  140. 

Artesian  wells,  151,  163. 

drift,  226. 

erosion,  231,  232,  234. 

brick,  237. 

limestone,.  335,  360,  377,  384. 

lime,  381,  382. 
Rainfall,  34,  128,  171. 
Randall,  elevations,  123,  213. 

Kettle  Range,  211. 
Randall,  Dr.,  531. 


Randolf,  583. 

elevations,  445. 

Lower  magnesian  limestone  in,  547. 

St.  Peters  sandstone  in,  556. 

Trenton  limestone  in,  558. 
Range,  689. 
Rantoul,  123. 
Raplin,  365. 
Rattlesnake  Rock,  575. 
Raymond,  123. 
Reconnoissance,  1875,  72. 
Red  Clay,  lower,  220,  221. 

upper,  225. 

modified,  225. 

soil,  193,  196. 
Reedsburg,  elevations,  446. 

quartzite,  517. 

Potsdam  sandstone,  532,  541. 
Reefs,  ancient  coral,  369. 
Relations  of  streams  on  opposite  sides  of 

Kettle  Range,  135. 
Report  of  1873,  5. 

of  1874,  45. 

of  1875,  67. 

on  Eastern  Wisconsin,  91. 

on  Central  Wisconsin,  407. 

on  Lead  Region,  643. 
Rhine,  elevations,  123,  223. 

drift,  211. 
Rib  Hill,  485,  489. 
Richfield,  123. 
Richmond,  cranberries,  186. 

drift,  206,  211. 
Richland,  355. 

Rio,  Potsdam  sandstone  in,  544. 
Ripon,  elevations,  123,  170. 

Lower  Magnesian,  274. 

Trenton  limestone  in,  301. 
Ripple  marks,  276,  319,  345. 
Roches  moutonees,  614. 
Roche-a-Cris,  540,  572. 
Rochester,  123. 

town  of,  140,  143,  169. 
Rock,  elevations  in  town  of,  123,  169. 

St.  Peters  sandstone  in,  287,  288. 

Galena  limestone  in,  308. 

Trenton  limestone  in,  297. 
Rock  Lake,  140,  215. 
Rock  River  Valley,  102,  129,  199,  202, 
492,  217. 

system,  129. 

east  branch,  135. 

water-power,  171. 
Rockla-nd.  121. 
Rockville,  356. 
Rocky  Run.  492. 
Reminder,  Dr.  C.,  84,  96,  284,  313. 
Rosendale,  123. 
Round  Lake,  140. 
Roxbury,  elevations,  440. 

Lower  Magnesian  in,  547. 
Rubicon  River,  136,  333. 
Rudolph,  564. 
Ruger,  E.,  171. 
Rush  Lake,  138,  275. 
Rushford,  Artesian  wells,  150,  159. 
Russel,  123. 


766 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


Rutland,  elevations,  170,  434. 
Trenton  limestone  in,  558. 


s. 


Salem,  123. 

Sandstone,  calcareous,  337, 

Potsdam,  257,  525,  668. 

St.  Peters,  235,  555,  675. 
Sapronite,  29. 

Sank  County,  579,  529,  532,  533,  534. 
Sank  City,  Lower  Magnesian,  548. 
Saukyille,  elevations,  123. 

Niagara  limestone  in,  368,  378,  379. 
Scapolite,  28. 
Schleswig,  123. 
Scott,  585. 

elevations,  124,  444. 

Lower  Magnesian  in,  547. 
Scoular,  James,  332. 
Scoville,  S,  155. 
Seed-Ore,  329. 
Selenite,  319. 

Seneca,  quartz-porphyry,  520. 
Sevastopol,  124. 
Seven  Mile  Creek,  310. 
Shaw,  S.,  8,  93. 
Shawano,  Lake,  130. 

county,  red  clay,  223. 

Lower  Magnesian   limestone  in,  271, 

280. 

Sheet,  definition,  670. 
Sheboygan,  elevations,  124. 

county,  140,  206,  209. 

Artesian  well,  151,  164. 

drift,  228. 

lime,  382. 

brick,  237. 

Niagara  limestone,  378,  379. 
Sheboygan  Falls,  elevations,  124. 

Niagara  limestone,  378. 
Sherman,  124. 
Shields,  elevations,  124,  170. 

Trenton  limestone,  301. 
Shopiere,  299. 
Shot-ore,  329. 

Shullsburg  District,  713,  747. 
Shumard,  Dr.  B.  F.,  596. 
Siderite,  29. 
Silicified  Fossils,  351. 
Silurian,    Lower,    Eastern    Wisconsin, 
257. 

Central  Wisconsin,  525. 

Lead  region,  668. 

Upper  Silurian,  327. 
Silver  Lake,  139,  140. 
Silver,  27. 
Single's  Mill,  489. 
Sinks,  206,  214,  661. 
Sinsinawa,  661. 
Smithsonite,  29,  694. 
Soils,  Central  Wisconsin,  449,  451,  599. 

Eastern  Wisconsin,  188,  316. 
Origin,  188. 
Descriptions,  190. 
Prairie  loam,  191,  196,  198. 


Soils,  Eastern  Wisconsin  —  continued. 
Lighter  marly  clay,  192,  198. 
Heavier  marly  clay,  192,  198. 
Red  marly  clay,  193,  196. 
Limestone  loam,  194,  198. 
Silicious  sandy,  195,  198. 
Calcareous  sandy,  195.  19?. 
Humus,  195,  196,  198. 
Alluvial,  196, 
Magnesian  character  of,  197. 

Lead  region,  663. 
Somers,  124. 
Spar,  29. 

Specular  ore,  330. 
Sphalerite.  28,  692. 
Springs,  30,  88,  658. 

Barnes,  147. 

Beloit  lodo- Magnesian,  146,  147. 

Bethesda,  32,  146,  147. 

Big  Spring,  145. 

Cedarburg,  148. 

Druecker's,  144. 

Dousman's,  32,  145. 

East  Troy,  32. 

Eureka,  32. 

Fountain,  146,  147. 

Gihon,  146,  147. 

Hackett's,  32. 

Horeb,  146,  147. 

Hygeia,  146,  147. 

Lowe's,  32,  147. 

Mineral  Rock,  32,  147. 

Mitchell's  142. 

Nemahbin,  32,  147. 

Oakton,  32,  147. 

Richmonds,  32,  147. 

Siloam,  32,  147. 

Schwickhart,  32. 

Sheridan,  147. 

Stowe's  145. 

Telulah,  148. 

White  Rock,  146,  147. 

Chalybeate,  148. 

Sulphur,  148. 

Travertine,  148. 

Trout,  149. 
Spring  Prairie,  124. 
Spring  Valley,  124..  125,  169. 
Springdale,  559. 
Springfield,  603. 

Elevations,  438. 

Lower  Magnesian  b'mestone  in,  547. 
Springvale,  elevations,  444. 

Lower  Magnesian  limestone  in,  547. 
Star,  Hon.  W.,  284. 
Sterling,  W.  C.,  328,  332. 
Steele.Pres.  G.  M.,  172. 
Stiles,  283. 
Stockbridge,  elevations,  125. 

Cincinnati  shales,  318. 

Iron  ore,  333. 

Analysis  of  limestone,  338. 
St.  Peters  Sandstone,  eastern  Wisconsin, 
285. 

Central  Wisconsin,  555. 

Lead  region,  675. 
Strise,  200,  201,  205,  625. 


INDEX. 


7C7 


Strong,  Moses,  6,  44,  46,  55,  64,  65,  66, 
71,  543,  560,  597,  609,  610,  643. 

Party  of,  1873,  9. 

Party  of,  1874,  55. 
Sturgeon  Bay,  204. 

Elevations,  125. 
Springs,  149. 

Cranberries,  186. 

Niagara  limestone,  346,  348,  352,  354, 
368,  372. 

Terraces,  228. 
Starin,  P.  J.,  106. 
Statistics,  of  zinc  ore,  742. 

of  lead  ore,  743. 
Stevens,  W.  C.,  93. 
Stevens  Point,  480,  530,  546,  564. 
Strikes,  464. 

Stratigraphical  Arrangement,  See  un- 
der the  several  formations. 
Sugar  Creek,  elevations,  125. 
Stream,  129,  136. 

Cranberries,  186. 

Peat,  243. 
Sulphides,  28. 
Sulphur,  27,  692. 
Summits,  etc.,  24. 

Elevations,  125. 

Cranberries,  186. 

Peat,  245. 
Sumpter,  590. 

Elevations,  446. 

Quartzite,  504,  518. 
Stunner,  125,  170. 
Sun  Prairie,  601. 

Elevations,  439. 
St.  Peters  Sandstone,  556. 
Swallow,  G.  C.,  51. 
Swoet,  K.  T.,  7,  49,  72,  235,  332, 412, 470, 

673,  680,  681,  689. 
Swezey,  G.  D.,  52,  93,  106. 
S wither,  definition,  690. 

T. 

Talc,  29. 
Taycheedah,  elevations,  125,  223. 

Springs,  149. 

Artesian  wells,  150,  154. 

Cincinnati  shale,  318. 

Niagara  limestone,  339,  340. 
Taylor,  Gov.  W.  R.,  71. 
Tetrahedrite,  20. 
Terraces,  228. 
Theresa,  springs,  149, 

Drift,  215. 

Rock  river,  135. 
Thiela,  H.  F.,  146. 
Thickness,  Potsdam,  257,  460,  528. 

Lower  Magnesian  limestone,  271,  460, 
514,  551. 

St.  Peters  sandstone,  460,  555. 

Trenton  limestone,  291,  460,  681. 

Galena  limestone,  307,  685. 

Cincinnati  shale,  315. 

Clinton  iron  ore,  330,  333,  334. 

Mayville  beds,  338. 

Byron  beds,  346. 


Thickness  —  continued. 

Lower  coral  beds,  351 . 

Upper  coral  beds,  353. 
Timber,  175,450,660. 
Tiff,  29. 
Tiles,  229. 
Till,  199-217. 
Toay,  James,  741. 
Topographical  characters. 

Potsdam,  533. 

Lower  Magnesian  limestone,  548 

St.  Peters  sandstone,  556. 

Trenton  limestone,  559. 
Topographical  maps,  647. 

Survey,  16. 
Topography. 

Eastern  Wisconsin,  of,  97-127. 

Central  Wisconsin,  of,  413-447,  453. 

Lead  region,  of,  643-652. 
Tourmaline,  29. 

Trains  of  bowlders,  202,  252,  253. 
Transition  beds,  298.  297,  287,  348,  542. 
Travertine,  144,  148,  318. 
Trenton,  elevations,  125. 

Trenton  limestone  in,  301. 
Trenton  limestone. 

Eastern  Wisconsin,  290,  305. 

Central  Wisconsin,  558. 

Lead  region,  680. 
Troy,  elevations,  125,  445. 

Lakes,  139. 

Troughs,  glacial,  130,  131.  139,  201. 
Trout  springs,  149. 
Turtle,  elevations,  125. 

Creek,  136. 

Lake,  139. 

Trenton  limestone,  299. 

Galena  limestone,  308. 
Twin  river,  east,  132. 
Two  Rivers,  elevations,  125. 

river,  132. 


u. 

Unconformability,  391,  462. 
Union,  elevations,  125,  126,  169. 

Trenton  limestone,  301. 
Utica,  elevations,  125. 


Y. 

Value,  see  economic  considerations. 
Vanuxem,  80. 

Vegetation,  native,  of  Central  Wisconsin, 
176-187. 

of  Central  Wisconsin,  449. 

of  Lead  region,  660. 
Vein,  denned,  690. 
Vernon,  elevations,  126. 
Verona,  elevations,  435. 

Trenton  limestone  in,  558. 

of  Lead  region,  660. 
Vienna,  elevation,  448. 

Lower  Magnesian  limestone,  547. 

St.  Peters  sandstone,  556. 


70S 


GEOLOGICAL  SURVEY  OF  WISCONSIN. 


w. 

Wad,  28. 

Walworth  county,  126,  131, 136, 139,  206, 
211,  342. 

town  of,  212,  213. 

springs  in,  149. 

Warren,  Gen.  G.  K.,  26,  421,  585. 
Waring.  Geo.  W..  160. 
AVa.shburn,  Gov,  C.  €.,  6.  71. 
Washington  .Bounty,  126,136,  140,  206. 
Wash  Dirt,  691. 
AVasley  Range,  742. 
Water.  2s. 
Water  power,  141,  170. 

of  Rock  river,  171. 

of  Fox  river,  172. 

of  Milwaukee  river,  174. 

of  Sheboygan  river,  174. 

of  Manitowoc  river,  174. 

of  Wolf,  Oconto  and  Peshtigo  rivers, 

173,  176. 

AVater  supply,  141. 
Water  lime.     See  Hydraulic  lime. 
Waterford,  126. 
Waterloo,  elevations,  126,  170. 

brick  at,  2:'.s. 

quartzite,  252-256.  _ 

Lower  magnesian  limestone  at,  271. 

St.  Peters  sandstone  in,  290. 

Trenton  limestone  in,  301. 
AVatertown,  elevations,  126. 

Artesian  wells,  150,  151,  160. 

brick,  238. 

lime,  308. 

Galena  limestone  near,  309. 
Watershed,  12*. 
Waubakee,  limestone  near,  392. 
AVaukesha,  county,  140,  206, 211, 316,  342. 

elevations  in  town  of,  126. 

springs,  144. 

limestone,  335,  357-360,  384. 

lime,  382. 

fossils  at,  372. 
AVaupun,  elevations,  126. 

building  stone,  308. 

Galena  limestone  at,  310. 
Wausau,  486,  488. 

Wauslmra  county,  529,  533,  541,  578. 
Wantoiua,  546. 
Wamyatosa,  elevations,  126,  127. 

Niagara  limestone  at,  365,  368,  372. 
Wayne,  elevations,  127. 

Rock  river  in,  135. 
AVernerite,  28. 
Wells,  Artesian,  149. 

in  Lead  Region,  658. 
West  Bend,  131. 

Elevations  in,  127. 
Westfleld,  elevations,  446. 

Quartzite,  504,  517. 

Potsdam  sandstone,  532. 
Westford,  elevations,  127,  170. 

Trenton  limestone  in,  304. 
West  Point,  586. 

Elevations,  446. 

Lower  Magnesian  limestone  in,  547. 

St.  Peters  sandstone  in,  556. 


AVestport,  602. 

Elevations,  439. 

Lower  Magnesian  limestone,  547,  555. 
Wheatland.  elevations,  127. 
Whitfleld,  Prof.  R.  P.,  93,  262,  263,  358, 

537,  554,  561,  585,  594. 
Whitefish  Bay,  399. 
White  river,  128,  129,  136,  203. 
Whitewater,  206. 

Elevations,  127,  213. 

Springs  near,  148,  149. 

Artesian  wells,  150.  162. 

Drift  at,  209,  211. 

Brick  tiles  and  pottery,  239. 

Peat  in,  242. 

Lime,  308. 

Galena  limestone  in,  309. 
Whitney,  Prof.  J.  D.,  57,  68,  69,  528,  559, 

560,  609,  622,  647,  667. 
Whitney's  Rapids,  466. 
Whitney's  Bluff,  319,  344. 
Whitemore,  D.  J.,  86,  400. 
Whittlesey,  Col.  C.,  69,  95,  206,  211,  631. 
AVight,  Dr.  O.  AV.,  67. 
AVilliarastown,  331,  340. 
AVilson,  J.,  Jr.,  maps  of,  13. 
Wilson,  J.  H.,  103,171. 
AVild's  well,  153 
AVilke  Lake,  140. 
Winchell,  Prof.  A.,  504,  596. 
AVinchell,  Prof,  N.  H.,  96,  204,  288. 
AVind  Lake,  000. 
AVindsor,  elevations,  440. 

Lower  Magnesian  limestone. 
Winfleld,  447,  593,  597. 
AVinkler,  C.,  35. 
AVinnebago  county. 

Potsdam  sandstone  in,  264, 

Lower  Magnesian  limestone,  271,277. 
Winneconne,  275. 
AViota  mining  district,  740. 
AVonewoc,  568. 
AVood,  Paul  B.,  106. 
Wood,  J.  W.,  595. 
AATood  county,  563,  461,  529,  541. 
Woodland,  532. 
Woodville,  127. 
Woodward,  S.  S.,  160. 
AArooster,  T.  C.,  8,  52,  93,  100. 
AVorrall,  Col.  Jos.,  103,  172. 
AA7orthen,  A.,  82. 

Wright,  Chas.  E.,  72,  73,  76,  520,  637. 
Wright,  N,  D.,  8,  93. 
Wrightstown,  127. 
Wyocena,  443. 

Y. 

Yellow  River  Valley,  490. 
York,  elevations,  441. 

Lower  Magnesian  limestone,  547. 
Yorkville,  127. 

Z. 

Zinc,  carbonate,  29,  683. 
bloom,  29. 
ore,  statistics,  742. 


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